The Ottam 05

DEPARTMI

MI1 BURE

THE OTTAM 05

Base of Peace Tower of the main building of the Parliament Buildings at Ottawa, showil~gthe use of Nepean s:indstone in the structure. The trimming stone used at the base and at il~tervnlsill the tower is another sandstone, from Sovn Scotia. CANADA DEPARTMENT OF MINES AND RESOURCES

MINES AND GEOLOGY BRANCH BUREAU OF GEOLOGY AND TOPOGRAPHY

GEO1,OGICAL SURVEY

MEMOIR 241

GEOLOGY OF THE OTTAWA-ST. LAWRENCE LOWLAND, ONTARIO AND QUEBEC

BY Alice E. Wilson

te Parliament Buildings at me in the structure. The OTTAWA ~alsin the tower is another EDMOND CLOUTIER 8 PRINTER TO THE KING'S MOST EXCELLENT MAJESTY 1946 Price, 66 cents No. 2474 f CONTENTS

Preface ...... V CHAPTER I

Introductiorl ...... 1 General statement ...... 1 Previorls history ...... I Field work and acknou~ledgments...... 4 CHAPTER I1

Genera) character of the area ...... 5 CHAPTER 111 Stratigraphy ...... enset ...... i Table of formations ...... 8 Precambrian ...... 9 Ordovician ...... 10 Beekmantown ...... 10 Nepean formittion ...... 10 March formation ...... 12 Oxford formation ...... 14 Correlation of the Beekmantown (Lower Ordovician) formations ...... 16 Cliazy ...... 17 Rockcliffe formation ...... 17 St . Martin formation ...... 19 Correlation of the Chazy formations ...... U) Black River and Trenton ...... 21 Ottawa formation ...... 21 Collingwood and Gloucester ...... 26 Eastview formation ...... 26 Billings formation ...... 25 Correlation of Eastview and Billings formations...... 28 1)undas-Lorraine ...... 28 Carlsbad formation ...... 28 Richmond ...... 30 Russell formation ...... 30 Queenston formation ...... 30 Quaternary ...... 31 Pleistocene ...... 31 Glacial deposits ...... 31 Champlain deposits ...... 31 Recent ...... 32 CHAPTER IV Structure ...... 33 CHAPTER V Economic geology ...... 36 Rock products ...... 36 Building stone ...... 36 Quarried stone ...... 36 Field stone ...... 38 Crushed stone ...... 38 Stone for cement ...... 39 Sand and gravel ...... 39 Stone for lime ...... 40 Abrasives materials ...... 40 Miscellaneous uses ...... 40 CONTENTS - Concluded Water ...... 41 Potable waters...... 41 Mineral springs ...... 42 Oil and gas ...... 44 CHAPTER VI Bibliography ...... 49 Geology ...... 49 Palaeontology ...... 55 The Ottawa-St. La 5,500 square miles lyin rence River and Otta~ ~ 1 Index ...... 61 larger province of the S formations that, in tur older ~recambrianroc city of Ottawa, and fo. Map 85%. Ottawa-Cor~~wall,Ontario and Quebec ...... In pocket geological study and p: 413A. Ottawa sheet, East Half ...... " " 414A. Ottawa sheet, West Half ...... " " The present acco Plate I. Nepean sandstone in the main building of the Houses of Parliament, extending over a ~eric Ottawa ...... Prontispiece time in connected for] 11. A. A boulder hill of Nepean sandstone, near Mirabel, Quebec ...... 45 IH. Oxford dolomite showing cryptozoons and characteristic weathering...... 45 of the area, and is illr 111. A. Sandstone lens in shale in Rockcliffe formation ...... 46 by two more detailed L B. Ottawa formation, showing natural profile of a drag on the down-faulted side includes a full bibliog of a fault, Governor Ray, Ottawa ...... tfi geology or palaeontol 1V. Thick limestone strata of the I,eray-Rockland beds of Ottawa formation. Quarry south of Rockland, Ontario...... 17 intended to serve a dl V. Heavy layers of Cobourg beds of the Ottawa formation as exposed in the Palaeozoic formations excavation for the Customs Building, Ottawa...... 48 bibliography for a se

Figure 1. Ottawa-St. Lawrence Lowland, showing its relation to the Canadian Shield , that will deal particul~ and the Adirondack Mountains ...... VI fauna of the Ottawa fc 2. Index of separate maps of Ottawa-St. Lawrence Lowland ...... 3 3. Faults affecting the Palseozoic rocks of the Ottawa-St. Lawrence Lowland. In pocket

OTTAWA,September 2 PREFACE

The Ottawa-St. Lawrence Lowland represents an area in Canada of some 5,500 square miles lying mainly between and west of the junction of St. Law- rence River and Ottawa River. It forms a characteristic part of the much larger province of the St. Lawrence Lowlands, underlain by flat-lying Paleeozoic formations that, in turn, rest unconformably on an eroded basement of much older Precambrian rocks. The Ottawa-St. Lawrence Lowland includes the city of Ottawa, and for more than a century has been subject to intermittent ...... In pocket geological study and palceontological investigations...... ' " ...... " '3 The present account is based largely on the author's own field work Parliament, extending over a period from 1925 to 1941, inclusive. It deals, for the first ...... 1"rontis~iece ...... 4.5 time in connected form, with the Paleeozoic geology and economic resources ic. weathering .... 15 of the area, and is illustrated by a general geological map of the region and ...... I(i by two more detailed maps of the area about the city of Ottawa. The memoir the down-faulted side includes a full bibliography of the many contributions concerned with the ...... 4Ci This is tf Ottawa formation. geology or paleeontology of the Ottawa-St. Lawrence Lowland...... 17 ! intended to serve a dual purpose, as a guide to future investigations of early on an exposed in the i Pal~eozoicformations in other parts of Canada, and as a convenient reference ...... 4s I bibliography for a series of presently planned Geological Survey Bulletins ) the Canadian Shield that will deal particularly with the identification and description of the prolific ...... vi ld ...... 3 fauna of the Ottawa formation. amence Lowland. In pocket

GEORGE HANSON, Chief Geologist, Geological Survey

OTTAWA,September 25, 1'945 Geology of th (

The Ottawa-St. La greater physiographic pr part of it, here describl basin occupies, altogethc lying between the Laure and the Adirondack Mo the Frontenac axis, an i rocks, which connects tl the Thousap? Islands border is defined by a 1 anticline', and which e- Quebec, south to the Adi sandstone, except near R brian rocks emerge thrc country. The Canadian part about 5,500 square mile: accompanying geological of the Pal=ozoic fo~mat Figure 1. Figure showing the position of the Ottawa-St. Lawrence 1,owland relative the basin extending west to adjacent areas of Precambrian rocks (in ruling). axis. The rnap-units used by recognizable disconft the confusion arising on formation and for the 1 hand, from the use of n are really faunal associ: several classifirations of

I11 1841 and 1842 S the Geological Survey, I hasin ~~nderprcsent rol Geology of the Ottawa-St. Lawrence Lowland, Ontario and Quebec

I LNTKODUCTION C;ENF:RAI, STATEMENT

The Ottawa-St. Lawrencc Lowland is a well-defiried basin within the greater physiographic province of the St. Lawrence Lowlands, and the greater part of it, here described, lies north of the International Boundary. The basin occupies, altogether, an area of some 7,900 square miles (See Figure 1) lying between the Laurentian Highlands of the Canadian Shield on the north and the Adirondack Mountains on the south. Its western margin is along the Frontenac axis, an irregular, northwesterly trending belt of Precambrian rocks, which connects the Canadian Shield with the Atiirondacks and forms !. the Thousand Islands where it crosses St. Lawrence River. The eastern border is defined by a lesser axis named by Logan (1863) the 'Beauharnois .! .! anticline', and which extends from the Canadian Shield near St. Jerome, Quebec, south to the Adirondacks. This axis is mantled with basal Pal~ozoic sandstone, except near ltigaud and the Lake of Two Mountains where Precam- brian rocks emerge through the sandstone to stand above the surrounding country. The Canadian part of the Ottawa-St. Lawrence Lowland has an area of about 5,500 square miles, most of which is included within the borders of the accompanying geological map (No. 8528, in pocket). The present discussion of the Palaeozoic foi-matiom, however, includes reference to the remainder of :nce Lowland relative the basin extending west to the Canadian Shield and southwest to the Frontenac 1g). axis. The map-units used in this report are defined by lithological changes and by recognizable disconformities. New names have been introduced to clear the confusion arising on the one hand from the use of the same name for a formation and for the period in which it was deposited, and, on the other hand, from the use of names of formations and members to designate what are really faunal associations. This confusion is particularly evident in the several classifications of the beds that constitute the Ottawa formation. I PREVIOUS HISTORY In 1841 and 1842 Sir William Logan, preparatory to his directorship of the Geological Survey, made brief reconnaissance explorations in parts of the basin under present consideration. He recorded some general observations and gathered some fossils. His Preliminary Report dated December 6, 1842, In 1895 N. J. G'wou? gives some description of the Ottawa and St. Lawrence Valleys. The fossils was assigned to study this collected were submitted to British geologists who "with cautious hesitation" but died the following W] pronounced that the wntaining strata belonged to Murchison's Lower Silurian several maps and reports 1 system. During the years IS9 In his Report of Progress for 1842, Logan outli~~edthe margin of the mapping of the Precamhri: Pal~ozoicrocks west of a line that extends northeast from Lake Champlain of the Pal~ozoicbasin. ). to Quebec City. He traced the basin west beyond the present city of Ottawa, rocks, and in 1897, after tl south to the Rideau Lakes and Brockville, and east again to Lake Champlain. of the main Palseozoic bnsi He then described the rocks at the southwest of the region as continuing west- in the several Annual ltr~ ward to the Mohawk Valley and recrossing the Canadian boundary at Kingston, from which point he outlined the boundaries of the rocks of central and western Ontario. Although he regarded all the Palaeozoic rocks of eastern and western Ontario as parts of one basin, it can be seer) that he recognized the existence of the Frontenac axis. In a succeeding report, for 1845-46, he gave a more detailed description of the Ottawa Valley, and though still a little vague about the Frontenac axis he recognized an eastern and a western area of Palaeozoic rocks. In 1851 Alexander Murray explored a part of the eastern area, using the New York nomenclature to describe the formations he encountered. He also recognized a number of the faults. In 1853 Murray ascended Ottawa and Bonnech2re Rivers, and in 1854 he traversed the Great Lakes, and, on his return to Ottawa Valley via Georgian Bay, discovered the Palaeozoic inliers bordering the valley of the upper Ottawa. Logan's 1863 report on the Geology of Canada inclutlcs scattered descriptions of the Palaeozoic formations within the Ottawa-St. Lawrence basin. In this report he first mentions the Beauharnois anticline, which marks the eastern boundary of the basin under discussion, though he describes it only in its southern part, from the International Boundary to the Lake of Two Mountains. The first map to include the Ottawa-St. Lawrence Lowland was issued in 1864 to accompany Logan's 1863 report. Four geological maps by R. W. Ells were issued by the Geological Survey in the years 1901 to 1906. These covered the Palzozoic lowland region and much more of the adjacent Pre- cambrian terrain. In 1906 the Geological Survey issued a more detailed map by Ells of the district immediately around the city of Ottawa. Since that date ~everalmaps have heen publishetl that include only small parts of the basin. Figure 2. Index of sepn In 1856 Elkanah Billings was appointed Palzontologist to the Geological rence Lowland: (1) 1 sheet (West Half!; ( Survey, and was responsible for the determination of fossils and the strati- 6628, L'Orignal; (61 graphy of the basin as represented in the 1863 report. In 1857 he visited and 710A, Prescott. described some of the Palzozoic inliers just beyond the northwest margin of the basin. From his appointment until his death in 1875 most of Billings' numerous publications contained tiescriptions of fossils from this region A number of later various geological aspect In 1874 anti 1875 H. G. Vennor ascended Ottawa River. He was concerned authors: H. M. Ami, n' mainly with the Precambrian rocks of the region, but in his refercnceto the Kindle and L. D. Rurli Palaeozoic formatioris Ile was the first to note the absence of the Potsdam and the Beekmantown from the base of the extreme end of the tongue of Ortlovician The Pleistocerle ana 1 rocks that extends up Ottawa Valley. Traces of the Beekmantown, but not is treated in this repor of the Potsdam, have since been found. Vennor describes outcrops of Chazy prior to 1863 he made 5~ limestone, which are now considered to be the base of the Ottawa limestone, of Canada of 1863 his 1 the Pamelia heds of Black liivcr age. *iography is morr. clr.ta dated L)ecenlber 6, 1842, 111 1895 N. J. G~roux,wllo lrad bcer~tlo~rig gc~ologlcal \+ark 111 Quebec, rice Valleys. The fossils was assigned to study thiq basin He was 'in the field' during 189.5 and 1896, with cautious hesitation" but died the following wi11tc.r HIS uncoml)leted norlc was incorporated in urchison'q Lower Silurian several maps and reports by R. W. Ells During the years IS91 a~ld1896 R. \V. Ells was asaigned to the study ant1 tlined the margirl of thc mapping of the Precambrian region bordering the northern and western margins st from Lake Champlaim of the Paleozoic basin. His surveys ~lece~sarilyiricluded some of tlre Palzozoir te present city of Ottawa, rocks, and in 1897, after the deatli of K..I. Giroux, he undertook the completion $,gainto Lake Champlain. of the main Paleozoic basin. .43 the work proceeded the rvsl~ltswere p~~hlished egion as continuing west- in tlrt. several Annual Reports of thc Geological S11rvt.y. an boundary at Kingston, 2ks of central and western ks of eastern and western 0 0 recognized the existence R A 1845-46, he gave a more i still a little vague about cestern area of Palaeozoic le eastern area, itsing the lc encountered. He also ~y ascended Ottawa and ireat Lakes, and, on his red the Palaeozoic inliers

L inclutles scattered des- awa-St. Lawrence basin. ticline, which marks the ugh he describes it only dry to the Lake of Two NEW YORK STATE nce Lowland was issued eological maps by R. W. L~S1901 to 1906. These ore of the adjacent Pre- ued a more detailed map G.S. C. Ottawa. Since that date small parts of the basin. Figure 2. Index of separate geological maps covering parts of the Ottawa-St. Law- ,ologist to the Geological rence Lowland: (1) Map 413A, Ottawa sheet (East Half); (2) Map 414A, Ottawa sheet (West Half); (3) Map 5888, Nepean; (4) Map 5878, Casselman; (5) Map of fossils and the strati- 6628, L'Orignal; (6) Map 661A, hfaxville; (7) Map 660A, Valleyfield; (8) Map In 1857 he visited and 710A. Prescott. the northwest margin of n 1875 most of Billings' Is from this region. A number of later papers, included in the Bibliography, dealing with various geological aspects of parts of the region, have been published by several iver. He was concerned authors: H. M. Ami, W. A. Johnston, P. E. Raymond, M. E. Wilson, E. M. ut in his reference to the Kindle and L. D. Burling, A. E. mrilson, and others. :nee of the Potsdam and the tongue of Ordovician The Pleistocene and Recent geology of the Ottawa-St. Lawrence Lowland Beekmantown, but not is treated in this report in a general way only. In most of Logan's reports :ribes outcrops of Chazy I prior to 1863 he made some reference to the surface deposits, but in the Geology )f the Ottawa limestone, of Canada of 1863 his treatment of Pleistocene and Recent geology and physiography is more detailed. In 1898, Ells described the sands and clays of the Ottawa basin, and in the same year W. J. Wilson published some notes on the Pleistocene geology of the district. In 1901 Ells described some ancient channels of Ottawa River, basing his conclusions on records of well borings. The first systematic study of the Pleistocene of a limited district within the region was carried on by Joseph Keele and W. A. Johnston for the XIIth International Geological Congress excursions. In 1916 Johnston discussed the various oscillations of sea-level in the Ottawa district during the latter part GENERA of Pleistocene time, and in 1916 he published a study and map of the Pleistocene and Recent deposits of the area. The surface of the Ot In 1922 E. J. Whittaker made a comparison of the fossil and present in places as a series of low invertebrate fauna of Mackay Lake, Ottawa, and in 1926 E. M. Kindle similarly level, is near the mouth of studied the fossil and modern diatoms of the present and late Lake Champlain Immediately to the north stages of the same lake. interrupted by steep, Prec saddle between these inlie mum elevation of 175 FIELD WORK AND ACKNOWLEDGMENTS towards the Adirondacks to an elevation of 250 fee The field work for this report was carried on from 1925 to 1941, with some that extends east and s interruptions. Within the area mapped (See Map 85211, in pocket) every elevation on its eastern I known outcrop of Palaeozoic rocks was visited and plotted. maximum of 500 feet at t Much of the bedrock is covered by unconsolidated glacial and marine Within the lowland sediments. The interpretation of the stratigraphy, the ranges of fossil species, solidated Quaternary de~ and the boundaries of formations as indicated on the Nepean, Prescott, Cassel- sures. Only near its nort man, L'Orignal, Rlaxville, and Valleyfield maps (Figure 2), are based upon ally flat-lying sediments, i field observations, the study of thicknesses obtained from many wells, and upon the construction of mortx than a hundred parallel and intersecting struc- The entire lowland is ture sections. drained by the upper St. tributaries. The St. Lav The writer wishes to express illdebtedrless to I. Gringorten, d. A. Calder, of the basin. In part of J. Lambert, and R. Lill for their able and untiring assistance during four truncates the Canadian consecutive field seasons, 1936 to 1939. Gratitude is also espressed for inforrn- point where the boundary atior~and courtesy from the managers of quarries and plants, garagemen, and within the lowland regic many other residents of the rrgion. higher elevation than the the low level of tlie Otta rivers. The older Palxozoic disturbed by faulting. 7 lies within a few miles of at a lower level because or near the Precambrial Laurentian Highland ant; the eastern quarter of thf adjacent to but considel the east-centre quarter t selves. On a part of tl abruptly on the north b3 in places to 1,100 feet ; Iwoad lowlancl, and, con Ottawa Rivcr cross ancl out around fault bl the city of Ottawa. FO slightly faulted trough lsoll publisl~edsome notes ":Is described some ancient In records of well borings. f a limited district withill I. .Johnston for the XIIth CHAPTER I1 1916 Johnston discussed trict during the latter part GENERAL CHARACTER OF THE AREA ~ndmap of the Pleistocene 1 The surface of the Ottawa-St. Lawrence Lowland rises gently to the west of the fossil and present 111 places as a series of low steps. The minimum elevation, 70 feet above sea- 326 E. M. Kindle similarly level, is near the mouth of Ottawa River along the eastern margin of the basin. and late Lake Champlain Immediately to thc north, along the 'Reauharnois anticline', the low floor is interrupted by steep, Precambrian inliers with an elevation of 600 feet. The saddle between these inliers and the Canadian Shield to the north has a minimum elevation of 175 feet. Southward along the Beauharnois anticline towards the Adirondacks the floor rises gradually from the 70-foot minimum 1925 to 1941, with some to an elevation of 250 feet, then abruptly to 600 feet, to a sandstone highland 852A, in pocket) every that extends east and south beyond the map-area. From the minimum dotted. elevation on its pastern margin the floor of the lowland gradually rises to a maximum of 500 feet at the Frontenac axis on the west. lated glacial ar1t1 marine 'le ranges of fossil species, Within the lowland region the Pal~ozoicbedrock is covered by uncon- Nepean, Prescott, Cassel- t solidated Quaternary deposits, or outcrops in low ridges and scattered expo- gure 2), are based upon sures. Only near its northern margin, where faulting has disturbed the origin- d from many wells, and ally flat-lying sediments, is any considerable thickness of bedrock exposed. el and intersecting struc- The entire lowland is a basirr roughly triangular or subquadrate in outline, L drained by the upper St. Lawre~lceand lower Ottawa Rivers and their several ;ringorten, .J. A. Calder, tributaries. The St. Lawrence flowing northeasterly crosses the western part assistance during four of the basin. In part of its course it forms the International Boundary and llso expressed for inform- truncates the Canadian part of the basin on the south and west. East of the ! plants, garagemen, and a point where the boundary changes to follow the 45th parallel the river continues i within the lowland region under discussion. The St. Lawrence flows at a higher elevation than the Ottawa. It falls over a long series of rapids, attaining the low level of the Ottawa only a short distance west of the junction of the rivers. The older Yaliixmoic formations bordering the St. Lawrence are not much disturbed by faulting. The height of land between the two rivers everywhere lies within a few miles of the St. Lawrence. Ottawa River, to the north, flows at a lower level because the region is down-faulted along a series of faults at or near the Precambrian margin. The expression of the break between the Laurentian Highland and the lowland region varies from place to place. Alqng the eastern quarter of the margin, a fault brings the oldest Palaeozoic formntlon adjacent to but considerably below the level of the Precambrian rocks. On the east-centre quarter the faulting occurs within the Palaeozoic rocks themselves. On a part of the western half, above Ottawa, the basin is limited abruptly on the north by the Eardley fault scarp, where the Precambrian rises in places to 1,100 feet above sea-level. In the western quarter there is no broad lowland, and, consequently, no clearly defined margin. Ottawa River crosses this irregular terrain along fault lines or flows in and out around fault blocks. Its comparative youth is well illustrated near the city of Ottawa. For some miles above the city it flows in an erosional or slightly faulted trough between the rocky banks of a low, plateau-like area; on the southwest side of the river the removal of the Ottawa limestone from the surface has exposed the weaker Rockcliffe shales and sandstones, and the river has widened its bed, forming Lake DeschCnes. Nearer the city it is again narrowed, traversing a complicated faulted zone of Ottawa limestone over which it flows in a series of rapids culminating in Chaudi4re Falls. Emerging from the confining banks of Ottawa limestone it again broadens somewhat, flowing less swiftly and depositing the sediments scoured from above the city. In March and Torbolton townships a low depression separates that part of the limestone-capped plateau on the west side of Ottawa River from the higher land to the south. The depression, evidently a former river channel, is now occupied by Constance Bay, Constance Creek, Constance Lake, Mud Lake, Shirley Creek, and Shirley Bay. A rise of less than 25 feet in the present The Ottawa-St. Lawn average water-level of the Ottawa would again make an island of cons. VI, age, with the possible ex( VII, and VIII, March and Torbolton tps., and at the same time would flood consider the latter to be of 1 another depression south of Lake DeschCnes, now drained by Watts, Still, The Ordovician formati01 and Water Creeks. Below Ottawa the river valley is outlined by terraces of River and Trenton, Utic clay and sand lying against Precambrian rocks on the north side, and, on the thickness is about 2,200 fc south, linking isolated bluffs of Ottawa limestone that mark the position of east to west. Of this thic some of the fault blocks. The summit of the bluffs, though higher in the is represented by 350 feet, Ottawa limestone section, has approximately the same elevation as the plateau- Ordovician by 950 feet of like banks above the city, and the elevation of their exposed bases is approximately that of river-level above the city. The strata have no g in the northern half of tl The features of the Ottawa-St. Lawrence Lowland record a sequence of fault blocks. Over the g Precambrian events followed by a very long period of erosion; a series of gently undulating, but th Palsozoic deposits later subjected to faulting; a second, long period of erosion; or on nearing the principa i glaciation; a last invasion and withdrawal of the sea; and subsequent elosion ! to present time. The deposition of the Palsozoic rocks and their lithological The Lower Ordovicia and structural features are considered in the following chapters. There is no 1 from the east. It deposi evidence of submergence during the later Palsozoic, Mesozoic, or Tertiary dolomitic limestone, and s times. withdrew to the east. The basin lies within one of the oldest settled parts of Ontario and western Between this emerge] Quebec, and has many historic landmarks connected with the struggles and interval during which roc1 early settlement of the country. Ottawa, the capital of the Dominion, is the age were laid down elsewh~ largest city, but there are a number of smaller, progressive cities and towns, were deposited in the 350 particularly along the St. Lawrence. Agriculture, especially dairy farming, turn by the deposition of has been the main industry for many years, but recently a rapid industrial of which is represented i~ growth has followed the increasing development of c.omparatively cheap i electric power. The development of the potential power of the rapids of the The Middle Ordovici International section of the St. 1,amrence should grtaatlp increase the population r deposited in this region 1 i and intlustries of the region. , the Montreal area, not lo] the brief subsequent eroc i the entire region of nor1 P Ordovician time advancb t er~teredthe lowland basil The initiation of U] Tlle preceding erosional Niddle and the base of where. Drill rccords ind hut there is no well-exp~ unconformity esists. T Lawrence basin consist c interbedded with shale a amount of shale indicatt the Ottawa limestone from .les and sandstones, and the 'ncs. Nearer the city it is I zone of Ottawa limestone n Chaudi&reFalls. Emerging again broadens somewhat, CHAPTER I11 :oured from above the city. ression separates that part STRATIGRAPHY of Ottawa River from the tly a former river channel, I GENERAL STATEMENT eek, Constance Lake, Mud I 3 than 25 feet in the present The Ottawa-St. Lawrence Lowland is underlain by rocks of Ordovician ake an island of cons. VI, 1 age, with the possible exception of the basal sandstone. Some authorities the same time would flood consider the latter to be of late Cambrian age, but the evidence is not conclusive. J drained by Watts, Still, The Ordovician formations include rocks of Beekmantown, Chazy, Black is outlined by terraces of River and Trenton, Utica, Lorraine, and Richmond age. The maximum he north side, and, on the thickness is about 2,200 fcet, though certain formations vary somewhat from that mark the position of east to %rest. Of this thickness the Lower Ordovician and possible Cambrian ~ffs,though higher in the is represented by 350 feet, the Middle Ordovician by 900 feet, and the Upper le elevation as the plateau- Ordovician by 950 feet of sediments. r exposed bases is approx- The strata have no general direction of dip and strike, and, particularly and record a sequence of I in the northern half of the region, are broken by faults and down-dropped fault blocks. Over the greater part of the basin the rocks are flat-lying or )d of erosion; a series of gently undulating, but they are tilted at varying angles in the fault blocks nd, long period of erosion; or on nearing the principal fault zones. t; and subsequent erosion )cks and their lithological The Lower Ordovician sediments were laid in a shallow sea transgressing 1g chapters. There is no from the east. It deposited the typical sequence of sand and dolomite or C, Mesozoic, or Tertiary dolomitic limestone, and some shale in the declining stages as the waters again withdrew to the east. ts of Ontario and western 3 with the struggles and Between this emergence and the next invasion there was a long erosional 1 of the Dominion, is the interval during which rocks of Lower Ordovician and early Middle Ordovician :ressive cities and towns, age were laid down elsewhere. Thus, some 700 feet of Beekmantown sediments .specially dairy farming, were deposited in the Montreal region, followed by an emergence, followed in :ently a rapid industrial turn by the deposition of 890 feet of Chazy rocks in Champlain Valley, none >f comparatively cheap of nrhicll is represented in the Ottawa-St. Lawrence Lowland. lwer of the rapids of the t The Middle Ordovician sediments are mainly of limestone and were first v increase the population deposited in this region when the Chazy sea spilled over into the basin from the Montreal area, not long before it, too, retreated again to the east. During the brief subsequent erosional interval there was evidently some warping of the entire region of norteheastern America, for the next invasion of Middle Ordovician time advanced around the south side of the Adirondacks and entered the lowland basin from the west across the Frontenac axis. The initiation of Upper Ordovician deposition is less certainly defined. The preceding erosional interval must have been short, for the top of the Middle and the base of the Upper Ordovician lacks no deposits known elsewhere. Drill records indicate an abrupt change in the nature of the limestone, but there is no well-exposed contact. In the Georgian Bay region a definite. unconformity exists. The Upper Ordovician sediments of the Ottawa-St.'/ Lawrence basin consist of shale, with the exception of a few feet of limestone interbedded with shale at the base and again at 100 feet from the toe. The amount of shale indicates that at no stage was the basin very deep. Even r * r TAB] during Richmond time, when thick beds of limestone were being deposited ,. in the Arctic regions and to the west and southwest, only minor quantities of limestone were laid in this basin. The initial invasion into the lowland in Period Upper Ordovician time was from the north, but later it combined with a contemporaneous invasion from the Gulf of Mexico. There is no evidence within the region of a later Yalaozoic invasion, but younger rocks may have been laid down and subsequently worn off during the long erosional interval that followed. It is a curious fact, however, that no trace of either Silurian or Devonian boulders have been found in the till, though every other type of rock is represented from the earliest Precambrian to the latest Ordovician. - An immense interval of unrecorded time elapsed between the withdrawai of the latest Ordovician sea and the beginning of the glacial period, for at

,. . pregent the irregularly eroded surface of the Ordovician and Precambrian rocks is overlain directly by unconsolidated Pleistocene deposits of glacial till and varved clays, and by marine beds of clay and sand from the post-glacial Champlain Sea. For practical mapping purposes and for use in the interpretation of well borings the formations to be described have been divided primarily upon a lithologic basis. In previous works the 'formations' within the larger time clivisions have been based upon fossils that were thought to be typical of Ordovician certain horizons. Further study of the fossils have shown that many formp or Cambrian have a longer range within the Ottawa limestone than at first supposed, theit. - I persistence or non-persistence largely depending upon local conditions. example, it is possible to map the Black River-Trenton 'formations' as the"Oj Precambrian have been defined on the bases of local lithology and of fossils cons.idercd to be .\rchsean ( ?) diagnostic. A section, however, constructed upon thicknesses as they have been estimated on these bases in several localities, when adjusted to meet the requirements of exposures, would present unreasonable variations of thicknesses within sediments of contini~ousdeposition.

It 1s not a purpose ( Era 1 Period 1 Sub-epoch I Formation i Description in ~tsrelationship to the - - complex bordering and Recent Alluvium gneisses, and quartzites, of granite, syenite, and ( Ce~~ozoic Quaternary Champlain Marine clay and sand Pleistocene of these areas of Precaml Till and varved clays only a few detailed inv

\ both general and detailec! Great unconformity of this report. Queenston Red shale Richmond As previously noted Russell Grey shale with heavy the basin of Palzeozoic fc interbedded dolomite to the east. It also evc -- by well borings, and outc Grey shale and sandy, rusty the Palaozoic rocks havc Paleozoic Ordovician Lorraine Carlsbad shales with thin dolomitic layers near top long tongues or ridges cbxtend southeasterly we1 Black shale with few feet of on the north. Both ou brown shale at base Aylmer plain, is limited Limestone with a little cast by a continuation / interbedded hale c~lc~vatiorlof morc. tllan I TABLE:OF FORMATION- Concluded stone were beirig deposited st, only minor quantities of -- vasion into the lowland in Era Period Sub-epoch For~natior~ Description

. later it combined with a -. - >. Discoi~formity ter I'alaeozoic invasion, but quently worn off during the Limestone with a little shale ious fact, however, that no and some sand at the base Lve been found in the till, Diseoi~formity I m the earliest Precambrian St. Martin Impllrr limesto~le -- I ed between the withdrawal Chazy Rockcliffe Shalc \\.it11 sandstone lenses 1 f the glacial period, for at - -. 1 dovician and Precambrian wene deposits of glacial till Disconforn~iij/ sand from the post-glacial Oxford Dolomite with a little shale at the top Beekluantown - - 1 the interpretatiol~of well March Interbedded sandstone and divided primarily upon a dolomite I 8ns' within the larger time Pep------. . . -- - thought to be typical of Ordovician Nepear~ Sandstone .e shown that many forms or Cambrian ban at first supposed, their -- -- pon local conditions. Greof unconformity enton 'formations' as thFor y - I of fossils considered to & Precambrian Grrnvillc Crystalline limestone, quart- Irchaean ( ?) zites, and metamorphic : tllicknesses as they havk rocks; associated grauite when adjusted to meet the and grani te-gneiss 1 nable variations of thick-

PRECAMBRIAK

It is not a purpose of this repurt to discuss Precambrian geology except I Description in its relationship to the Palzeozoic formations. In general, the Precambrian - complex bordering and within the basin consists of crystalline limestones, Alluvium gneisses, and quartzites, intruded, deformed, and metamorphosed by bodies Marine clay and sand of granite, syenite, and other igneous rocks. The existing reports and maps 1 - of these areas of Precambrian rocks are based mainly on reconnaissance work, I Till and varved clays only a few detailed investigations having been undertaken. References to -. both general and detailed studies are included in the Bibliography, Chapter VI of this report. 1 Red shale - As previously noted the Precambrian complex forms the boundaries of Grey shale with heavy the basin of Palzozoic formations to the north and west, and to some extent interbedded dolomite to the east. It also everywhere underlies the later sediments, as evidenced Grey shale and sandy, rusty , by well brings, and outcrops as isolated exposures within the lowland wherever shales with thin dolomitic the Pal~ozoicrocks have been eroded from above it. In some places it forms layers near top long tongues or ridges within the margins of the basin. Two such tongues extend southeasterly well into the Palzeozoic basin from the Canadian Shield Black shale with few feet of brown shale at base on the north. Both owe their position to faulting. One, adjacent to the Aylmer plain, is limited on the southwest by the Eardley fault, and on the 1,imestone with a little east by a continuation of the Gloucester fault. The ridge slopes from an interbedded shale elevation of more than 1,100 feet to pass under unconsolidated surface deposits at about 325 feet. The other, a low ridge reaching an elevation of 425 to 450 Throughout, it is m feet, connects with the Shield in the region of Fitzroy Harbour, and extends p. 430), in an analysis of across Torbolton and March townships to Nepean township. Its greatest it averages 99.31 per cen elevation is along its southwest edge where it is cut off by the Hazeldean fault. has been found to the e: On its northeast side, and at its terminus in Nepean township, it passes beneath are rarely exposed. Of the basal sandstone of the Pal~ozoic. Other ridges, which do not owe their merate with quartzite pe origin to faulting, project into the Pal~ozoicbasin from its southwest boundary quartzite pebbles of mor. west of Brockville, and from the western margin. They existed before the sand. Over considerable later marine invasions took place, and have been exposed by erosion. At the but masses with angular terminus of the two ridges in the Brockville region are a few scattered knobs marine and terrestrial cc in line with the ridges. The knobs appear to be the higher tops of ridges that of changing shore sanc persist beneath the thin Palseozoic cover. In addition, a number of isolated asymmetric ripple-marks knobs of the Precambrian rocks are exposed well within the basin; all of these . knobs are of white quartzite, except that some granitic rock as well as quartzite Some grains show a SI is uncovered in one place slightly west and about 8 miles north of Brockville. material throughout is s in places is of calcium ca cofiesion is so slight that there are many occurrenc ORDOVICIAN zitc from a fraction of ar, sions. One of the thick road about 3 miles east : these lenses are disconn~ free circulation of water. Nepean Formation There are no adeq Ottawa-St. Lawrence ba: Definition and Contacts. The Nepean sandstone is that formation that section would be charac overlies the unevenly eroded Precambrian floor of most of the Ottawa-St. few inches thick are ovt. Lawrence basin, and in turn is overlain by the interbedded sandy dolomite one place thinning out I and sandstone of the March formation. The unconformity at the lower contact represents a long period of erosion. The contact is nowhere actually The Nepean sandst( exposed, but in lot 3, con. 11, March tp., the sandstone is separated from-the it is laid. From an ex Precambrian rocks by a few feet of drift. At its margin the sandstone appears sandstones over a wide i to conform to the slope of the Precambrian surface and may have extended minerals found in the sa over it. The sandstone exposure is only a few inches thick, but increases to the gneisses themselves several feet and becomes more nearly horizontal within 20 to 30 yards. The was derived from the gl upper limit of the Nepean is placed arbitrarily at the base of the first dolomitic brian rocks. or calcareous bed. This contact is conformable; nowhere is there a trace of a break in the sedimentation. As here defined the Nepean is a homogeneous Thickness. The th formation easily recognizable in borings, but less readily detected in the field least 500 feet. Over th unless the upper limit is exposed. It includes all the sandstone in this region between the unevenly formerly designated as Potsdam, and, at the top, beds that Raymond (1913, there are evidences of sc p. 139) considered to be "reworketl Potsdam" and correlative with the Theresa mum thickness yet foun of New York. The definition of the upper contact obviates the consideration about 16 miles east of of a variously placed, doubtful contact between a Cambrian and an margin, a drill passed Ordovician formation. the Precambrian. This Palzozoic trough or to The formation is named from Nepean township, where the large quarries or to both combined. lie from which the stone was taken for the Parliament Building of Canada, iq not possible, as no w ant1 for many other large government anti other buildings (See Plate I). Distribution. The Description. Thc Ncpean as a whole is a cream-coloured sandstone, formations of the basil weathering grey, and nlottlccl with irregular rust spots. Towards the south- # overlap it and extend west margin, and to some extent in the eastern part of the basin, it has a rocks. The exposnres decidedly red tinge. of the main basin and : an elevation of 425 to'450 Throughout, it is made up of a coarse yuartz sand. Harding (1931, roy Harbour, and extends p. GO), in an analysis of the sandstone from various localitic~s,has found that n township. Its greatest it averages 99.31 per cent silica (Si02). .ipproxinlately the same pcbrccntage off by the Hazeldean fault. has been found to the east of the area near Bcauharnois. The basal layers township, it passes beneath are rarely exposed. Of the few known outcrops qome show beds of conglo- .s, which do not owe their merate with quartzite pebbles 1 inch to 3 inches in diameter; others contain om its southwest boundary I quartzite pbbles of more uniform pea-size; still others are of coarse-grained They existed before the sand. Over considerable areas of the exposed sandstone the grains arc rounded, .posed by erosion. At the but masses with angular grains are not uncommon, indicating pcrllaps both are a few scattered knobs marine and terrestrial conditions, probahly representing a sliore relationship : higher tops of ridges that of changing shore sands and ocean sand-bars. Numerous, well-defined, tion, a number of isolated asymmetric ripple-marks are R~~O~~ICI.evitlencc of near shore current conditions. thin the basin; all of these , .ic rock as well as quartzite Some grains show a secondary growth of quartz, and much of the cementing miles north of Brockville. material throughout is siliceous. Near the top of the formation the cement in places is of calcium carbonate, or of rust-staining iron oxide. In places the I cohesion is so slight that the grains can be separatrd by the fingers. Again there are many occurrences of thin, streaky, disconnected lenses of pure quart- ! zitc from a fraction of an inch to 2 feet thick and with irregular lateral dimen- sions. One of the thicker quartzite lenses is exposed in a field north of the road about 3 miles east and south of Belle RiviGre, Quebec. So far as known these lenses are disconnected, and have little or no effect in preventing the free circulation of water. There are no adequate sections of the Nepean formatior1 within the Ottawa-St. Lawrence basin, and deposition has been so irregular that no single ne is that formation that section would bc characteristic of the region as a whole. In places beds a f most of the Ottawa-St. ? few inches thick are overlain by beds that may be from 2 to 5 feet thick, in terbedded sandy dolomite one place thinning out laterally to a few inches. nconformity at the lower ontact is nowhere actually The Nepean sandstone is derived from the Precambrian rocks over which tone is separated from the it is laid. From an examination of the Precambrian gneisses and of these rgin the sandstone appears i sandstones over a wide area Harding (1931, p. 436) noted that all of the heavy e and may have extended minerals found in the sandstone were also in the gneisses. He concluded that hes thick, but increases to I the gneisses themselves were sedimentary in origin, and that the sandstone ! thin 20 to 30 yards. The I was derived from the gneisses rather than directly from the igneous Precam- :base of the first dolomitic brian rocks. #whereis there a trace of a Nepean is a homogeneous Thickness. The thickness of tlie Nepean varies from a few inches to at :adily detected in the field least 500 feet. Over the main part of the basin the sandstone fills in valleys .ae sandstone in this region between the unevenly eroded Precambrian base beneath, and in addition )eds that Raymond (1913, there are evidences of some dune-like deposition of the sand itstlf. The maxi- orrelative with the Theresa mum thickness yet found in wells at Ottawa is 280 feet, but at Silica, Quebec, obviates the consideration about 16 miles east of Lachute and about 2 miles south of thePrecambrian possible Cambrian and an margin, a drill passed through 500 feet of Nepean sandstone without reaching the Precambrian. This unusual thickness may be due to the filling of a pre- Palzeozoic trough or to a buried fault scarp near the Precambrian boundary, >, where the large quarries or to both combined. Comparison with thicknesses farther south and east nent Building of Canada, is not possible, as no well has penetrated to the Precambrian. ~ildings(See Plate I). Distribution. The Nepean everywhere underlies younger Palaeozoic :ream-coIoured sandstone, formations of the basin, except in the northwest, where the younger strata pots. Towards the south- overlap it and extend up Ottawa Valley, resting directly upon Precambrian ,art of the basin, it has a rocks. The exposures of the Nepean occur, therefore, around the margins of the main basin and about a few protruding Precambrian knobs.

Chapter VI of this report. Isolated outcrops show that the greatest area of the Nepean sandstone underlying the unconsolidated Pleistocene sediments is a broad band in the 1

L southern half of the greater part of th~basin, along the margin of the Beau- from the Nepean sandsto harnois axis, where the younger Palaeozoic rocks have been eroded. The dolomite, is to be seen on continuity of this wide band is broken farther north by several fault blocks the March is placed arbitr near Rigaud and by the adjacent Precambrian outliers. Within this faulted ity. The formation is he] area the narrowed and interrupted band occurs farther west than in the un- eristics are persistent thro disturbed area, and in the case of the Rigaud Mountain block it is represented zone. The formation is by an additional isolated outcrop at the uplifted western tip, lying against where good exposures occ Ottawa limestone. North of the faulted area the formation resumes its normal position between the Precambrian and the succeeding March formation. Description. The M: and sandy dolomite or b, A few, quite isolated outcrops are present on tlie northern margin of the The sand grains are large. basin in pockets or narrow strips adhering to the Precambrian rocks, but in Some of the thick dolomit most of this area the formation is cut off by faults. filled with large crystals I In the southwestern and western margin of the basin the Nepean lies transition from the Nepea against the Precambrian of the Frontenac axis in pockets and bands between being most evident at the ridges, and is preserved in patches westward across the southern part of this up, where dolomite is ma axis. Within the western margin one small outcrop occurs against a Pre- 18 inches. cambrian knob on the upthrow side of the fault running southwest of Paken- Thickness. No corn ham. The most westerly outcrop found within the basin is several miles At one locality, lot 18, c west of Almonte, and the most northerly a few miles north of Carp. both top and bottom are ( On the uptlirow sidta of the Hazeldean fault the Nepean formation lies in a thickness of 25 to 30 fc its nornlal position against the northeast margin of the Precambrian tongue to indicate that it beeor that extcsnds from Fitzroy Harbour into Nepean township. the formation is still thic Only o~rcexposure of tlie Nepean was found well within the basin, on the Because the format upthrow side of the Gloucester fault. It appears about a mile south and a tend to vary, depending : little east of I,ttitrim, and extends as a narrow band for about 10 miles, cut off of the basin sand would by the fault on one side arrcl elsewhere passing under the succeeding March whereas limestone an(1 dq formation. eastern areas. Fa~lttncct~d Correlation. Tllc only identifiable species found in the area is a small lit~guloitlshell described as Lingulella acuminutu Conrad. There Distribution. The ( are also a nurn1)e-t of tracks, sbrne having a width of 3 to 4 inches, made presum- than at the margins, a1 ably by some animal. In addition, the formation contains curious concret- gressively younger form: ionary structures of inorganic origin. Most of these are cylindrical, or flattened the outer Precambrian b cylinders, with their maxiriirlm diameters ranging from a few inches to several lies the Nepean and wit feet. Others have irregular constrictions along their length: still others are the March ex osures is 11 nodule-like. axis, but fartR er north, Rigaud Mountain. No A discussion of the corrclation of tlie Ncpcan sandstone is given later in formation must be prcso connection with that of the nZarch ant1 Oxford forniations, because the Nepean and Oxford outcrops a; sandstone, as liere defined, includes beds that have been correlated with western tip of the 1)lock. formations in NCWYork State of both late Cambrian and early Ordovician age. Along the northern March exposures is brok arch Formation formation is brought to fault blocks. IIefirtitio~r c~nd ('ontucts. The March formation lies above the Nepean sandstone anti I,elow the Oxfort-l formation. In a few places its base rests The March is wirlc unconformably upon Preeanlbrian knobs that protrude above the Nepean the basin from the Broc santlstonc; elsewhere both contacts are conformable. The lower contact is cambrian ridges projecl placed arbitrarily at the lowcst dolomitic layer. It is easily recognized in becomes narro\\ towarc well borings, but is more difficult to find in the field, because the lower basal Carletort Place, and thcb tlolomitic layer is rarely esposecl and the interbeddetl resistant sandstone village of Pakcnham. layers arc widely exposed and rc~semblcthe Nepean. No outcrop was found outcrop on tllc. northwc sllowing the ra;tct contact, h11t a typical sl~ccrssio~r,with few interr~iptions, irrm of tlrc* \csa cb\tc*~~tlvtl :the margin of the Beau- frolli Nepea11 sandstone into the alternating illarch santlstonc arid sandy have been eroderl. The dolomite, is to be seen on lot 34, con. VI, Nepean tp. The upper contact of 11 by several fault blocks the March is placed arbitrarily above the last occurrence of sand in any cluant- iers. Within this faulted ity. The formation is here consitlered as a lithologic unit, because its charact- .her west than in the un- eristics are persistent tl~roughoutthe area, and it is a well-ktiown water-bearing ain block it is represented zone. The formation is named from March township, Carlcton county, western tip, lying against where good exposures occur. mation resumes its normal lg March formation. Description. Tl~eMarch formation consists of alternating grey saridsto~~c. and sandy doloniite or blue-grey dolomite, all weathering dark rusty brown. northern margin of the The sand grains are large, generally rounded, and comnlonly Iooscly cemented. 'recambrian rocks, but in Some of the thick dolomite beds contain pockets, I inch to 3 inches in diameter, filled with large crystals of pink or white calcite. Tlle Sorlnatio~lrepresents a he basin the Nepean lies transition from the Nepean sandstone to the Oxfortl dolomite, the sand content xkets and bands between being most evident at tllc haw. The lower hecls are 2 to 23 feet thick. Higher the southern part of this up, where tlolomitc. is morcx prc~valcnt,the hcds vary in thiek~l~ssfrom 8 to op occurs against a Pre- 18 inches. ining southwest of Paken- lie basin is several miles Thickness. No completc sectio~i of the 1\Iarcli formatio~~i, csxposed. i north of Carp. At one locality, lot 18, con. 111, Nrpean tp., some 23 feet are t~uposed,but both top and bottom arc covered. Well borings in and arountl Ottawa indicatc Nepean formation lies in a thickness of 25 to 30 feet in this part of thc basin. There is sonlc cvidenccb ' the Precambriari tongue to indicate that it becomes thicker to the east, ant1 well records show that Pnship. the formation is still thicker cast of the Reauharnois axis. 11 within the basin, on the Because the formation is a shallow-water tlch~~osit,its thickness woulcl ibout a mile south and a tend to vary, depending llpon the sandy material available. Near the margins for about 10 miles, cut off of the basin sand would probably form a consitlerahlc part of tlle sediment, ler the succeeding March whereas limestone and dolomite wol~ldhe deposited in thc decsper, ec,ntral and eastern areas. species found in the area wminata Conrad. There Distrib~~tion.The Ottawa-St. Lawrence basil^ ih deeper at the centrc to 4 inches, made presum- than at the margins, and, consequently, where untlisturbed hy faults, pro- contains curious concret- gressively younger formations are exposctl in roughly concentric bands within Ire cylindrical, or flattened the outer Precambrian boundary. Next to the Prccamhrian within the basin )m a few inches to several lies the Nepean and within that the March. The concentric relationship of ,ir length; still others are the March ex osures is maintainetl along the southern part of the Reauharnois axis, but fart! er north, like the Nepean, it is interrupted by faulting about Rigaud Mountain. No outcrops are revealed in the faulted blocks, but the andstone is given later in formation must be present on the Rigaud Mountai~lblock between the Nepean tions, because the Nepean and Oxford outcrops against Rigaud Mountain ant1 again on the uptilted Lve been correlated with western tip of the block. and early Ordovician age. Along the northern margin of the basin the co~itinuityof the band of March exposures is broken by faulting. Outcrops are few and isolated. The formation is brought to the surface or buried by the irregular tilting of thr fault blocks. n lies above the Nepean few places its base rests The March is widely exposed in thc southwestern and western part of trude above the Nepean the basin from the Brockville area north, where it surrounds or tops the Pre- e. The lower contact is cambrian ridges projecting into the basin. The band of March exposures [t is easily recognized in becomes narrow towartls its northern limit. Outcrops are isolated around L, because the lower basal Carleton Place, and the farthest nortli exposure seen on this margin is in the dded resistant sandstone village of Pakenham. But a few isolated, thick, arenaceous dolomite beds . No outcrop was found outcrop on the northwest extremity of Calumet Island, ant1 indicate that an I, with few interruptions, arm of the sea extencled farther north and west 11p Ottawa Valley. North and east of the Hazeldean fault, on the upthrow side, the March, on the road about 13 mil( like the Nepean, is repeated in its normal position relative to the Precambrian. Another area occurs in cc The farthegt north exposure in this irregular area is about 12 mlles south of At the latter locality the Dunrobin. 8 to 10 inches in diametel quartz in places contain Two exposures occur well within the basin: one, in Mountain township, irregular sheets of variab probably is exposed because it covers a Precambrian knob; the other borders resists weathering and st: the Nepean sandstone outcrop southeast of Leitrim on the upthrow side of the Gloucester fault. Towards the wester overlaps Nepean and M. Fauna and Correlation. Fossils found within the formation indicate a very impure, with much r Lower Ordovician age. These interbedded sandstone and dolomitic layers ments, and all weather a were designated by Logan as the Transitional beds. The correlation of the These beds have been cc Nepean, March, and succeeding Oxford formations is given after the discussion quantity of sand and the of the Lower Ordovician (Beekmantown) formations. Surface outcrops and ville, Ontario, but none of Oxford Formation Thickness. It is po~ ness of the Oxford only Definition ut~clC'oritacts. The Oxford forlnation lies above the March ant1 northern part of the map is succeeded by the Rockcliffe. Over the greater part of the Lowland the in thickness towards the lower contact is placed arbitkarily above thc last stratum of sand in the March and at Carlsbad the Oxfc formation. It is unconformable ~vliereit surrounds the Precambrian knobs east of Carlsbad penetrat that protrutle above the March formation. Towards tlie northwest, the where the older formatiol Oxford is thought to overlap the Nepean and the March, and to lie uncon- thinner, being bevelled L formably upon the Precambrian. The contact with the March can bc recogn- block no well shows the ized in borings, but is more difficult to dcfinc in the field. Natural sections ? & method of surface measu showing the gradation of sand content are rare, ant1 large areal exposures of

resistant dolomite may or may not be srlcceedetl by sandy dolomites in covered Distribution. The ( areas. The upper contact is unconformable, arid can bc recognized readily March formations, illustl both in borings and in the outcrops. occurring in a band of val The Oxforcl formation ii nametl from Osfortl township, Greuville county, and broken border of the Ontario, wherc it is widely exposed. The same formation was called 'Beau- to the west of the March harnois' by Itaynlond (1913, p. 140). who usetl the name only once. The first part, but narrowing irrei of the castern Ontario areas to br revised by the present writer was that covered exposure is interrupted by the Ottawa sheet, and a new name was chosen because it was not known in its exposure a little far at that time whethcr the Oxford heds were iclentical with those of the original to the older format;o~l~ type area at Beauharnois canal. As the ~)rcsentmap indicates, the formation isolated and irregular, d IS much more widely spread in Oxford ant1 tlie adjacent townships, and as of the basin. the building of the new Beauliarnois canal has co\~credsomcl of the type area, As previously ment the name 'Oxford' is here retained. shallow. Within the C Description. Thc Oxfortl Formatiol~ 1s mostly a thick-bctlda-1 rusty the St. Lawrence from weathering dolomite. In plnc(.s it chaugeh Interally to limestone. *any of Farther north and west the dolomitic heds contain llarti spherical masses, from 6 inches to 2 feet in square miles, having a I diametet., that weather concentrically (Platc I1 B). They have been considered part of that area. In variously as concretions or as algal growths called 'cryptozoons'. In the the projecting or burie central and eastern part of the basin there is some shale at the top of the knobs. The field of ex] formation. Some of thcse upper, more shaly beds contain imperfectly spheroid the north, then patchy, or ellipsoid masses of more compact shale, 1 inch to 18 inches in diameter, western margin of the b which when weathered out leave shallon., basin-like depressions. The more Pakenham, outcrops oct shaly layers arc very dark grey and weather rr~sty. As in the Rlarcll formation, Nepean and March forn some of the lower thick tlolonilte beds contain pockets from 1 inch to 3 inches north of the Precambri in diameter, filled with large pink or white calcite crystals. M'here the Oxford Nepean township. Thc lies against or ovcrlaps Precambrian knobs the dolomite contains pebbles and Almonte and east of G hoirltlrrs of quartz 11~)to 10 or 12 illchcs long. One such rsposure can hc seen farther up Ottawa 'a1 ~pthrowside, the March, on the road about 1i niiles east of Oxford Statio~l,Oxford township, Ontario. ative to the Precambrian. Another area occurs in con. 111, GodmancheSker tp., Huntillgdon co.,Quebec. about 12 miles south of At the latter locality the dolomite also is honeycombed with irregular cavities 8 to 10 inches in diameter, lined with large quartz crystals or with anlorphous quartz in places containing dark chert. Quartz also occurs here in thin, ., in &lountain township, irregular sheets of variable thickness, or along vertical joint ~lanes,where it knob; the other borders resists weathering and stands out in relief. on the upthrow side of Towards the wester11 edge of thr basin, where the Oxford formation overlaps Nepean and March beds, the dolomite is still thick bedded,but is 1 he formation indicate a very impure, with much mud and some sand. Some beds break into platy frag- ne and dolomitic layers ments, and all a brighter yellow than in the eastern part of the basin. The correlation of the qiven after the discussion These beds have been considered Oxford, not March. because of tht. small quantity of sand and the large proportion of dolomite. Surface outcrops and low sections are numerous, especially near filerrick- ville, Ontario, but none of them reveals more than a small part of the formation. f Thickness. It is possible to obtain accurate measurements of the thick- i ness of the Oxford only within the large down-faulted block in the central ies ab0x.e tlie March ancl i )art of the Lowland the northern part of the mapped area. Within these limits it evidently increased um of sand in the March in thickness towards the east. At Ottawa wells show a thickness of 240 feet the Precambrian knobs and at Carlsbad the Oxford and hfarcli together are 350 feet thick. No wells erds the northwest, the east of Carlsbad penetrate the formation, but on the extreme east of the basin, [arch, and to lie uncon- where the older formations rise towards the Beauliarnois axis, it again becomes lie March can be recogn- thinner, being bevelled by erosion. To the west of the great central faulted field. Natural sections block no well shows the exact thickness, but, calculated by the less accurate large areal exposures of method of surface measurements, there is an appreciable decrease in thickness. ~dydolomites in covered The distributioll of the Oxford, as of the Nepean and n be recognized readily Distribution. March formations, illustrates the basin-like character of the region, exposures i occurring in a band of varying width around the basin, lying within the irregular nsliip, Grerlville county, and broken border of the older formations. On the east it forms a broad strip )ation was called 'Beau- f to the west of the March formation, averaging 12 miles in width inthe southern ne only once. The first part, but narrowing irregularly to the north. Similarly, the continuity of its writer was that covered exposure is interrupted by the faulting around Rigaud Mountain, resulting Zause it was not known in its exposure a little farther west where it maintains the same position relative .it11 those of the original to the older formations. Its occurrence, also, on the northern margin is indicates, the formatiorl isolated and irregular, due to the tilting of the fault blocks along that edge icent townships, and as of the basin. 1 some of the type area, As previously mentioned, the western side of the basin was probably shallow. Within the Canadian part, the Oxford formation outcrops along a thick-bedded, rusty the St. Lawrence from Iroquois almost to Brockville, with one interruption. to limestone. Many of Farther north and west ~t .occupies an irregular area of some hundreds of m 6 inches to 2 feet in square miles, having a maxlmum width of at least 50 miles in the southern *eyhave been considered part of that area. In places it lies in irregular depressions and patches between 'cryptozoons'. In the the projecting or buried Precambrian ridges, and between isolated buried shale at the top of the knobs. The field of exposure,.very wide in the south, becomes narrower to iin imperfectly spheroid the north, then patchy, then disappears entirely. In one small area nearthe 18 inches in diameter, western margin of the basln on the upthrow side of the fault southeast from Iepressions. The more Pakenham, outcrops occur just northeast of a Nepeari outcrop. It, like the in the March formation, Nepean and March formations, maintains its relative position to the east and from 1 inch to 3 inches north of the Precambrian ridge across Torbolton and March townships to als. Where the Oxford t t Nepean township. The western edge of the Oxford area is exposed north of te contains pebbles and Almonte and east of Galetta. The Beekmantown sea, however, penetrated :h exposure can be seen farther up Ottawa Valley, as indicated by three, small, widely separated outcrops, one about 9 miles north of Arnprior, another along Bonnech6re is that the sandstone wa: River at Douglas, and a third at Eganville. On the extreme western tip of phase of an advancing sea Allumette Island, north and west of Pembroke, some loose, rusty weathering The March formatio blocks of dolomite were seen that seem to have come from a near-by exposure, Nepean sandstone, was co perhaps under the river. They may be from basal Ottawa (Pamelia) beds, of New York, and conside but their thickness and density suggest the Oxford formation. Ontario. The position oj Fauna and Correlation. The presence of Ophilet~,Eccdiomphalus, Hor- name is now restricted motoma, and other forms is indicative of an early Ordovician age. The correl- locality in New York. F ation of this and the two preceding formations follows. The Oxford formatio of the area the same spc Correlation of the Beekmantown (Lower Ordot~ician)Pormationa March into the Oxford. few fossils not found wit Although it is not impossible that some Upper Cambrian sandstone is areas the Beekmantown : present, it is probable that the Nepean-March-Oxford sediments represent 2,000 feet respectively. continuous deposition in early Beekmantown time. It is even probable that part of this sectiov is rep in the western part of the basin the basal sandstone was laid down during deposition of some of the Oxford dolomite in the east. The invading sea, moving progressively westward over the Precambrian base, might have sufficient carbonates for deposition in its eastern part while depositing clastie material on its western shoreline. A static and a later retiring sea might The ilarne 'hylmer' result in concentration and deposition of carbonates directly upon the Pre- as represented in Ottawa cambrian rocks in the almost land-locked area of the upper Ottawa River the Aylmer - shale wit1 Valley. shows that these divisio Ottawa and St. Lawren The lithologic characteristics of the Nepean, March, antl Oxford fornlatiol~s I widespread distribution, ' suggest a normal succession produced by an encroaching shallow sea, grading as two formations. Thc from sandstone into interbedded sandstone and dolomite, and then into dolo- Rockcliffe, from Rockcl; mite, capped in some districts by the more impure shaly beds that probably border Ottawa River. 1 represent either a further shallowing or a withdrawal of the sea from the hasirt. its best tlevclopment is tc There is nowhere any evidence of a break in sedimentation. ,(% The Nepean has been called the Potsdam, ant1 correlated with the formation of that name in New York State where it is regarded as Upper Cambrian in age. The correlation and, consequently, the age have been based upon a L)eJinitiori UIL~('o~tl few fossils and upon the high silica content, which suggests an extended period i~n11in turn is overlain h of erosion antl dissolution of original feldspars. As indicated previously, the in the central and (,aster fossils are limited to the tracks of some unknown creatures and to a linguloid an(] dolomites of the bas; form, Lingzclella acuminata. Most of the tracks occur near Beauharnois, of the Rockcliffe with thc Quebec. One, near Perth, Ontario, and a very few from New York are also by a difference in litholc cited. It is felt that they are too indefinite for correlatioll. The gelins Lin- (lolomite may be seen il gulella has been cited from New York, Vermont, Virginia, Iliisconsin, Minrlcb- exhibit only sandstone 1 sota, ant1 Tennessee, from both the Cambrian and the Lowclr Ordovieiar~. sandstone is more resist It is rather too generalized a genus to be a. basis for exact correlation. Itr heen brought up by the eastern Ontario Lingulella acuminata has been found both in the sandstorlc. of the basin. In an aha layers and in a sandy limestone. No other fossils were found at the samcb the lighter grey, col~glol locality, but elsewhere such beds yield Ophileta compacts, Eccliomphal~~scalci- IIPOI~ the dark, rusty ferua, and other Lower Ordovician forms. The absence of feldspars may hc exposures of the contact accounted for by Harding's conclusions as to the tlerivation of the sandston<. of the ItockclifTe herotfl from Prccambrian sedimentary gneiss, not tlircctly from thr Precambriarl In the pasture cast of t igneous rocks. As stated elsewhere, there is no evidence of unconformity coriformity represents, 1 within the sandstone, though it is recognized that an unconformity between of the younger Beek~nal sand laid upon sand might be difficult to detect. The Nepean sandstone, forniity reprt.sents the then, may or may not have been deposited at the same time as the Potsdani ('hamplain area; the clel of New York, and within the Nepean itself therc is no definite c.vidtlnre that w(linlc,nts; the complet it is of Uppc~rCambrian age. The possibility is rcrognizctl, I)ut the probability ('lrnxy tinlc., il~l

Dark shale ...... 4 also found. The evidence ti Dark shale with some sand ...... 2.0 Dark, calcareous beds with large grains, almost pebbles, weathering C. plena. This evidence is grey ...... 1.1 that the two forms never oc -- techia- -- orientalis "arose fron Total thickness ...... 21% plications at an early stage' Covered (base of St. Martin) ...... 10 Roekcl

To the west of the large central expanse and separated from it by older formations, brought up by the Gloucester and Hazeldean faults, is an isolated area The upper contact i of Ottawa limestone of considerable extent, which occupies the northwest of the uppermost limestc corner of the Ottawa-St. Lawrence basin. The area is cut by faults into three the formation underlies 1 slices, and the underlying Beekmantown is repeated by two faults radiating Rideau River from Ottaw from near Pakenham. On each slice the Ottawa formation on its western Description. The E: margin overlaps the Beekmantown. Besides these larger areas there are four, shale. The limestone is small, isolated tracts of Ottawa limestone occurring in grabens from 7 to 18 crystals. It is thick bed, miles long, and 2 to 8 miles wide, namely, northwest of Arnprior, northwest upward to thinner beds of Renfrew, on Allumette Island and the surrounding country, and in a horse- rock types weather rusty shoe expanse extending from the Fourth ChQte of the BonnechGre to Lake Its presence has been de DorC and to Eganville, and five small remnants, at Calabogie Lake, Ashdad, northwest of Esmonde, Lake Clear, and southwest of Killaloe. Thickness. The Eas Correlation. The Ottawa formation comprises those beds usually called Ottawa. It apparently Black River, with its three members : Pamelia, Lowville, and Leray; and Trenton, ever occurred west of the with its four members: Rockland, Hull, Sherman Fall, and Cobourg. Distribution. The E Originally the entire formation, exclusive of the lowest mw and a few beds of it are ex] Pamelia, was included under the term 'Trenton'. Later, when the fo sil Ontario, another outcrop content was better known, the succession was discussed under the 'Trenton are several scattered expc and Black River groups', indicating that the various authors recognized a 13 and 14, cons. I11 and lithological unit though palzeontologically some gradation was evident, and in Pleistocene deposits cove Ontario the terminology of New York State was applied. In recent years in of the Ottawa formation, New York State the term 'Mohawkian' has been substituted in place of 'Trenton view at most is not wides and Black River groups'. The Pam~lia,originally excluded from the 'Trenton- Black River group' was first studied in New York State, where diagnostic Correlation. The co4 fossils were not found, and where the contact with the formation below it is of the Billings, when the concealed. It is there considered to be of Chazy age. Raymond (1912, p. 353) first introduced the name into Ontario. He correlated with the New York Pamelia similar beds at Kingston and in Ottawa Valley that lay above the topmost Chazy formation and which later he (1913, p. 141) assigned to Definition and Conta the Black River group, from its fossil content. The Black River, including the Eastview and below the Pamelia of Ontario,was divided into three and the Trenton into four unit embracing the top s members, really beds differentiated mainly by faunal associations. On the cester age. The lower cc accompanying map (No. 8528) the approximate boundaries of these associa- the uppermost limestone 1 ations ('members') are shown in dotted lines in order to correlate as nearly and wells, though there a as possible the beds upon which palaeontologists have done detailed work. the contact. The upper c The Ottawa formation, then, is correlated with the Pamelia and Mo- to detect because the ch. hawkian of New York, and with rocks of Black River-Trenton age in the cuttings of wells, and the Montreal, central, and western Ontario areas. Rocks of this age have not crossing the Ottawa-Mor yet been found in the northern regions of Canada. near the contact. It sht bands of dolomitic rock.

COLLINGWOOD.~ND GLOUCESTER The name 'Billings' Ottawa, where the forma Eastview Formation Description. The B few feet weather brown Definition and Contacts. The Eastview is a thin formation that overlies black, fissile shales. The the Ottawa limestone and is covered by the Billings. The lower contact is The best to be seen is in not exposed, but it is thought to be disconformable, because, though the beds have the same dip as the formation beneath, there is a change in the texture Thickness. The exa and colour of the rock, and, where exposed, the topmost beds of the Ottawa One well a short distanc limestone are somewhat weathered. It may be noted in this connection that Billings black shale with Sproule (1936) has found the base lying unconformably upon both lower and not far from the first but 1 upper beds of Black River-Trenton age on Manitoulin Island. at a depth of 203 feet. i 260 to 300 feet .d from it by older form- faults, is an isolated area The upper contact is conformable, and is placed arbitrarily at the top of the uppermost limestone bed. The name 'Eastview' is chosen because occupies the northwest the formation underlies the western edge of the village of Eastview, across s cut by faults into three by two faults radiating Rideau River from Ottawa. ormation on its western Description. The Eastview is composed of limestone interbedded with rger areas there are four, shale. The limestone is dark grey and fine-grained, with some large calcite in grabens from 7 to 18 crystals. It is thick bedded at the base with shaly partings, and gives place it of Arnprior, northwest upward to thinner beds with more shale, the latter dark and friable. Both : country, and in a horse- rock types weather rusty. No section is exposed, and even outcrops are rare. tlie BonnechZre to Lake Its presence has been detected by wells and excavations within tlie city of Calabogie Lake, Ashdad, Ottawa. Killaloe. Thickness. The Eastview has a maximum thickness of about 20 feet at those beds usually called Ottawa. It apparently thins out and disappears towards the east. If it >, and Leray ; and Trenton, ever occurred west of the Glouccstrr fault it has been eroded. 11, and Cobourg. Distribution. The Eastvicw formation is founct in excavations at Ottawa the lowest member, the and a few beds of it are exposed 011 the east bank of Kideau River. At Lemieux, Later, when the fossil Ontario, another outcrop is revealed in Nation River, at low water. There tssed under the 'Trenton are several scattered exposures of the shale above it between Ottawa and lots )us authors recognized a 13 and 14, cons. I11 and IV, North Plantagenet tp., and it is presumed that ation was evident, and in Pleistocene deposits cover the Eastview lying between this shale and the top died. In recent years in of the Ottawa formation, which outcrops within a short distance. The East- ituted in place of 'Trenton view at most is not widespread. cluded from the 'Trenton- : State, where diagnostic Correlation. The correlation of thc Eastview will be discussed with that the formation below it is of the Billings, when the ages of both formations are cor~sideredtogether. r. age. Raymond (1912, correlated with the New Billings Formutiotc wa Valley that lay above 1913, p. 141) assigned to Definition and Contucts. The Billings is that formation that lies above Le Black River, including the Eastview and below the grey shales of the Carlsbad. It is a lithological d the Trenton into four unit embracing the top shales of Collingwood age and all the shales of Glou- la1 associations. On the tester age. The lower contact is conformable, and is placed arbitrarily above undaries of these associa- the uppermost limestone of the Eastview. It has only been seen in excavations ler to correlate as nearly and wells, though there are a number of exposures of the shale a few feet above e done detailed work. the contact. The upper contact, too, appears to be conformable, but is difficult th the Pamelia and Mo- to detect because the change to grey shale is not clearly defined in the fresh tiver-Trenton age in the cuttings of wells, and the contact is nowhere exposed. An outcrop in a stream cks of this age have not crossing the Ottawa-Morrisburg road, south of Ellwood, is thought to be very near the contact. It shows the black Billings shale with a few intercalated bands of dolomitic rock. The name 'Billings' is chosen from that of Billings Bridge, a suburb of Ottawa, where the formation outcrops in the cutting of a stream. Description. The Billings is a shale formation throughout. The lower few feet weather brown and pass imperceptibly upward into thick beds of n formation that overlies black, fissile shales. There are a number of exposures but no complete sections. gs. The lower contact is The best to be seen is in Bear Creek, con. 111, Cumberland tp., Ontario. because, though the beds is a change in the texture Thickness. The exact thickness of the Billings formation is not known. )most beds of the Ottawa One well a short distance east of Billings Bridge penetrated 255 feet of the ed in this connection that Billings black shale without reaching the Eastview formation. Another well tbly upon both lower and not far from the first but on the other side of a minor fault reached the Eastview lin Island.. at a depth of 203 feet. The Billings formation probably has a thickness of 1 260 to 300 feet Distribution. The Billings is not widespread within the basin. Its Russell formation. Neit region of exposure forms a somewhat horseshoe-shaped area with its curved , thought from the dip oi tip lying under part of Ottawa. One arm extending southward IS cut off by From the nature of the B the Gloucester fault; the other extends eastward, cutcropping in Green Creek. on the Ottawa-Morrisbul An outcrop still farther east, in Bear Creek, demonstrates that the formation a quarry about half a mil' continues eastward though offset by one of the many faults. That it once is gradual. The position covered a much larger area is shown by four isolated outcrops; east of Ham- for there are no exposurt mond, east of Clarence Creek, west of Plantagenet, and at St. Isidore de shale, the contact is diffic Prescott. A well at Fournier reveals that the formation underlies heavy Pleistocene deposits in that district. A deep well at Carl record of the formation, : Description. The C Correlation of Eastview and Billings Formations ' I! some impure limestone 01 The Eastview and Billings formations of the Ottawa-St. Lawrence Lowland , show local variations con; represent a continuous sequence of beds, but are distinctive lithologically. section, compiled from sc Together they make up the former Collingwood and Gloucester of the basin, consists of interbedded 1 but the division between the two is different. The Eastview and Billings are overlain by beds of clear defined by lithology, the Eastview being limestone interbedded with shale, more rusty weathering, and the Billings all shale. The terms Collingwood and Gloucester are retained small sand content, ant! c as time terms. out. Originally the Collingwood was defined by Raymond (1911 and 1913) Exposures of some I as limestone and shale with the trilobite Ogygites latimarginatus Hall (cana- in a cre~kthat crosses tl densis Chapman) as the diagnostic fossil. Later this trilobite, associated Billings Bridge. North with an otherwise Trenton fauna, was found in 90 feet of thick-bedded, grey Billings shale. Higher 1 limestone in the Georgian Bay region. Parks (1928) lowered the Trenton- outcrop of Carlsbad sep: Ccllingwood contact to include these thick-bedded, grey limestones, limiting It consists of interbeddt- the upper boundary of tlie Collingwood by a Triarthrus that admittedly is South of this secontl roa found below the Collingwood-Gloucester contact as well as above it. On this the overlying grey, fissil basis the Collingwood embraces thick-bedded, grey limestone, dark, fine- bedded shale and rusty grained limtstone with shale, and at the top 15 feet or more of brown weathering of the shale has beer1 .see I shale, with lower and upper contacts indefinite. The thick-bedded, grey Thickness. The m: limestone Parks called Lower Collingwood, and the limestone interbedded with about 500 to 550 feet. shale, with the upper 15 feet or more of shale, Upper Collingwood. In the with the Billings below Ottawa-St. Lawrence Lowland the black, fissile shales above the Collingwood certain from well cuttin remained Gloucester, as defined by daymond. Because of the variability combined Billings and I of the boundaries antl the several t pes of lithology embraced by the term qhows 800 feet. 'Collingwood', antl the inclusion in ; of the 15 feet or more of shale more closely allied to the Gloucester abox , it is felt that a lithological definition of Distribution. The the formations is more reasonable ; ~d practical in the Ottawa-St. Lawrence large down-dropped blot Lowland. The Eastview, then, is to be correlated Q-ith the lower part of basin, protected hy thc Raymond's original Collingwood and with most of the Upper Collingwood of the upthrow side west o Georgian Bay as defined by Parks. The Billings is correlated with the Glou- dropped block. It occr~ cester plus the 15 feet or more of shale originally included in the Collingwood i~hout8 miles widc. Fr5 and lying above the uppermost limestone of the Eastview. The black shale it extends a little south I is also found in central Ontario near Whitby: in the Eastern Arctic; on Baffin is overlain by younger ra Island and on Grenfel Tickle, T,abratlor. Correlation. The (' L)undas of central Onta~ Foerste has concluded i Quebec were dcl)osited Carlsbad Formatio7r separate basin. Fossiliferous outcro Definition and Contacts. The Carlsbad is the shale formation of the 1 that the lowest beds of Ottawa-St. Lawrence area that lies above the Billings and is overlain by the from thta St. 1,awrcnrc. ; within the basin. Its Russell formation. Neither lower nor upper contact is c,xposcd, but it 1s ped area with its curved thought from the dip of the outcrops that both contacts are conformable. : southward is cut off by From the nature of the Billings shale in the highest exposure mentioned above cropping in Green Creek. on the Ottawa-Morrisburg road, and from the basal Carlsbad beds as seen in trates that the formation a quarry about half a mile east of Billings Bridge, it is thought that the change ny faults. That it once is gradual. The position and nature of the upper contact is even less certain, 1 outcrops; east of Ham- for there are no exposures near it, and, as the formation abovc. is also largely t, and at St. Isidore de shale, the contact is difficult to detect in well cuttings. rmation underlies heavy A deep well at Carlsbad Springs, Ontario, has given the most complete record of the formation, and the name is chosen from that of the village. Description. The Carlsbad formation is tlominantly grey shale, witit 5ome impure limestone or dolomitic bands and a little sand. The few outcrops wa-St. Lawrence Lowland show local variations common to shallow or near-shore deposits. A generalized distinctive lithologically. section, compiled from scatt~r~tloutcrops and a limited number of well borings, i Gloucester of the basin, consists of interbedded dark shale and rusty weathering bands of dolomitc Eastview and Billings are overlain by beds of clear, grey, fissile sliales, 1%-llich,in turn, are succeeded by interbedded with shale, more rusty weathc,ring, thin, dolomitic bantis arid shalc, in places having a td Gloucester are retained small sand content, and overlain hy marc sl~alc. Shale predominates throughout. lymo~ld (1911 and 1913) Exposures of soiric of these. phases can see11 in an interrupted section ztimarginatus Hall (cana- in a crerk that crosses the road about midway hetween Hurdman Bridge and this trilobite, associated Billings Bridge. North of the roatf, in the creek bed, is a small exposure of eet of thick-bedded, grey Billings shale. Higher up in the creek and just north of the nest road is an !8) lowered the Trenton- outcrop of Carlsbad separated from the Billings exposure by a covered area. grey limestones, limiting It consists of interbeddrd shale arid thin, rusty weathering barids of dolomite. rthrus that admittedly is South of this second road and ahout 500 feet east of the creek is a quarry in vell as above it. On this the overlying grey, fissile shales. '4bove this again, at I'eitrim, is the inter- y limestone, dark, fine- bedded shale and rusty weathering dolomitc \i~ithsome sand. No exposure more of brown weathering of the shale has bcen seen higlicr than this. The thick-bedded, grey nestone interbedded with Thickness. The maximuni thickness of the Carlsbacl is cstinlated at )er Collingwood. In the about 500 to 550 fect. As stated above, the exact positio~lsof its contacts .s above the Collingwood with the Billings below ant1 the Russell formation above are difficult to as- certain from well cuttings. The well at Carlsbacl Springs shows 600 feet of .cause of the variability combined Billings and Carlshatl, ancl another \veil farther east, near Vars, y embraced by the term t or more of shale more shows 800 feet. I lithological definition of Distribution. The Carlsbacl occurs only in the southwest part of tlic the Ottawa-St. Lawrence large down-dropped block of the eastern half of thc northern margin of the with the lower part of basin, protected by the older, morc resistant rocks brought to the surface on he Upper Collingwood of the upthrow side west of the Gloucester fault and by the tilting of the down- :orrelated with the Glou- dropped block. It occupies less than 160 square miles in the form of a band luded in the Collingwood about 8 miles wide. From its western edge, just south of the city of Ottawa, stview. The black shale it extends a little south of east for about 20 miles. A small area in the centre Eastern Arctic; on Baffin is overlain by younger rocks. Correlation. The Carlsbad may be correlated in a general way with the Dundas of central Ontario and with the 'Lorraine' of Nicolet Valley, Quebec. Foerste has concluded that the 'Lorraine' sediments of eastern Ontario and Quebec were deposited contemporaneously with those of New York, but in a separate basin. Fossiliferous outcrops are few, but a comparison of the fauna suggests shale formation of the that the lowest beds' of the Dundas and the 'Lorraine' of Quebec are midking qs and is overlain by the from the St. Lawrence area. The Whitella fauna, characteristic of the lowest Dundas horizon, is lacking in the basal Carlsbad, and only long range fossils Russell, where the uptur occur in both. Foerste (1916) has divided the Quebrc 'Lorraine' into four not cester fault. very clearly defined faunal zones, which, from the top to the bottom, he named the Pholadomorpha, Proetus, Lept~na,and Cryptolithus zoncs, respectively. Thickness. Estimatt No species from the Cryptolithus zone has been found in the basal Carlsbad. - indicate a thickness of ab It seems probable, then, that the Carlsbad represents sediments deposited combined. Many years some time after the beginning of Lorraine time. The Billings formation was referred to above, passed deposited in a sea that invaded the basin from the Arctic. The Carlsbad, shale at the top of the R on the other hand, is the most northern representative of a later invasion from Distribution. The ( the south. It is reasonable to suppose that some sediments were deposited north of Russell, Ontaric to the south before that invasion reached this area. the down-faulted block 1 truncated by the Glouce: Correlation. The Qi at the type locality in thc of these red shales east c Russell Formation Definition und Go~~tacts.The Russell formation overlies the Carlsbad shales and in turn is overlain by tlle Queenston. Both contacts are thought to be conformable, but neither of them is anywhere exposed, nor are there The superficial depo wells penetrating the formation. except in so far as they 2 The Russell formation is named from the township of Russell in which zoic rocks and the limit it occurs. bances that took place il Description. The Russell co~isistsof grey shale and interbedded, heavy, Pleistocene and Rec rusty weathering, dolomitic limestone. The grey shale has been seen only rine and fluvial muds a1 in diggings from a few surface wells. The thick-bedded, dolomitic limestone thickness from nil t,o 200 outcrops in the bed of a creek, about lot 24, con. VII, Cumberland tp., Ont., where they fill in the un and fossiliferous blocks a few feet higher in the section are strewn around shallow Palaeozoic depositio excavations, now overgrown, on lots 25 to 28, con. VIII, Cu~nberlandtp. emergence. If there wc Thickness. The thickness of the Russell formation is riot ktrowrl, but it they were eroded during must be very thin to occupy the limited space brtwecrl the highest known Carlsbad ant1 the lowest knolvn Queenston bedh. Distribution. The Iinssell formation occupies a very small area mwth and west of Itussell village, in the southwest corner of the clown-faulted block on the eastern half of the northern margin of the basin. It forms a narrow, circular rim arountf the rriargilis of the succeeding formation. Thin, irregular depc Correlation. Tlrc Iiussc~llformation may I,t. rorrc,latccl \\-it11 the Meaford I in the higher levels of th of the Georgian Bay arca. Much thicker, terminal bury to Cornwall (Joh~ (J~cernstoriFormation expose stratified gravels particularly in the cen Definition and Contacts. The Queenston forlnation overlies the Russell. laeozoic rocks or Pleisto It represents the latest Ordovician sediments in Ontario, and in the Ottawa- lakes and rivers during St. Lawrence basin is overlain by Pleistocene deposits. The lower contact is not exposed, but is thought to he conformable. The upper contact, exposed in several places, is very irregular, tlle unconforrnity rel~resrntingthe passage of all later Palzozoic, Mesozoic, :1nd Tertiary time. In the central an( Description. The formation is a red shale, occasionally strcaked or marine shells and fish I mottled grey-green. The best outcrop is in a quarry about 4 miles north in some places, bury tl of Russell, Ontario, where from 8 to 10 feet of it are exposed. Another out- beaches are found at ve crop, easy of access, occurs in tlrc hctl of Caqtor River, ahout 2 miles w~stof p. 5) on Kings Moi~nf rud only long range fossils I Russell, where tlir. upturned edgrs of the shale mark the course of the Glou- )cc 'Lorraine' into four not rester fault. 1) to the bottom, he named lithus zonc s, respectively. Thickness. Estimates based on a 11r11nberof intersecting structure sections ~ndin the l~asalCarlsbad. indicate a thickness of about 100 feet for the Russell and Queenston formations sents sediments deposited combined. Many years ago a boring put down in the quarry north of Russell, 'he Billings formation was referred to above, passed through 70 feet of shale, but this may have included ie Arctic. The Carlsbad, shale at the top of the Russell. ve of a later invasion from sectimcnts were deposited Dist~ibution. The Queenston occurs only in one small area west and north of Russell, Ontario, in a small basin at the extreme southwest corner of the down-faulted block mentioned below. The southern tip of the trough is truncated by the Gloucester fault. Correlation. The Queenston is identified with the formation of that name at the type locality in the Niagara Peninsula. It is the only deposit in Ontario of these red shales east of Credit River Valley.

on overlies the Carlsbad QUATERNARY Both contacts are thought re exposed, nor are there The superficial deposits were not a part of the investigation of this report except in so far as they are involved in the discussion of the underlying Palaeo- nship of Russell in which zoic rocks and the limit of their distribution is a result of the structural disturbances that took place in Palzozoic times. and interbedded, heavy, Pleistocene and Recent scdimcnts of till, late marine deposits, and lacust- shale has been seen only rine and fluvial muds and sands succeed the Ordovician rocks. They vary in dded, dolomitic limestone thickness from nil to 200 feet where they lie in boulder hills and sand dunes and 11, Cumberland tp., Ont., where they fill in the unevennesses of tilted blocks or erosional surfaces. are strewn around shallow 4111, Cumherland tp. Palaeozoic deposition within the basin was followed by a long period of emergence. If there were any Palaeozoic rocks younger than the Queenston tion is not known, but it they were eroded during that time. tween the highest known

a very small area north of the down-faulted block asin. It forms a narrow7, Glacial Deposits rmation. related with thc Mcaford Thin, irregular deposits of till and a few eskers overlie Palzozoic sediments in the higher levels of the western and in some of the central parts of the basin. Much thicker, terminal moraines and drumlins occur on the east from Hawkes- bury to Cornwall (Johnston, 1916, p. 3). Many sections of glacial material expose stratified gravels sorted by glacial streams. In some areas of the basin, tion overlies the Russell. particularly in the central and eastern parts, varved clays lie upon the Pa- iario, and in the Ottawa- laeozoic rocks or Pleistocene till, and bear witness to the presence of marginal 'sits. The lower contact lakes and rivers during the retreat of the ice-sheet. le upper contact, exposed representing the passage Champlain Deposits

rr In the central and eastern part of the basin, sand and clay containing occasionally streaked or marine shells and fish remains lie either directly upon the Palaeozoic rocks or, rry about 4 miles north Marine e exposed. Another out- in some places, bury thinly spread glacial debris, and boulder hills. .er, about 2 miles westof beaches are found at various levels, the highest being 690 feet (Johnston, 1916, p. 5) on Kings Mountain northwest of Hull. Most of the evidence of the and St. Lawrence Rivers in the western part of the"basin. *?rn The great weight of ice in Pleistocene time depressed the northern part of the continent, which was slow to recover its normal position after the withdrawal of the ice. During this period a gulf of the Atlantic Ocean penetrated the Greater St. Lawrence Lowland ancl inundated the Ottawa-St. Lawrence basin. Fresh water gave place to brackish, antl brackish water to salt water. The northern boundary of the invasion was defined largely by the zone of faulting along the Paleozoic-Precambrian border. This sea, known as the Champlain Sea, never transgressed far over the Canadian Shield, stopped The original uniform c by a wall where the Precambrian rocks rose abruptly above the Paleozoic St. Lawrence Lowland ha? basin, along the Eardley fault west of Gatineau Valley, and also east of Papi- Of these, the ~rincipalset neauville, where, to the north of the present Ottawa River, a scarp rises above east-southeast trend with , the highest beach. Between tlic~sepoints, where thc faulting lies within the Towards the west of the Palzeozoic rocks, the Precambrian formations to the north rise with a gentle south 60 degrees east. 1 monoclinal slope, and a hay of the Cllamplain Sea pr91)ably penetratecl farther true east. The general p north over the low Precambrian levrls of the country now clraineti by Gatineau from a centre but from an and Li6vre Rivers and to a lesser degree hy Blanche and North Nation Rivers. part of the basin (Figure : Along the southwestern margin of tl1e lowland the Champlain Sea penetrateti beyond the boundaries of the hasin over the Frontenac axis nearly to T,ak~ Most of the lesser set Ontario. The southern boundary lay ill New York Statc,. by the primary faults. T to the north of east. The faulting within confined to the northern the International Bounc Recent cleposith are ulade 11p of lacustrij~cn1arl.s ~.t.plett.wit11 fossils and boundary of the present alluvial sediments. Thc exposeti Pal~ozoicrocks antl the unconsolidated Precambrian rocks. glacial and marine sediments have been considerably modified by more recent Due to the location o erosion along Ottawa and St. Lan-rcncc Hi~rrsantf their long, winding tri- to the Precambrian rocks butaries. East of Papineauvillc by the Grenville fault, w upthrow side to the nortl region because only the But thc throw of the fau hy surface observations. of the present Precambri stone, which means either in a sinking area. The to the downthrow side su along a former fault in tl The second sectioll some 35 to 40 miles. In ern edge of the Paleozoic lying with a gentle mon broken region. The third section ex approximately 35 miles. 13eozoic sediments cxtenc primary faults here par; on the northeast abrup direction. On the sout: fault of lesser throw sep gher I;ii~cl t)c,twrcLrtOtta~a hasi 11. c~prehhc~lt11(. t~ortl~clr~~part nal position after the wit])- Atlantic Oceari penetrateci I the 0ttaw:t-St. Lawrcncc. CHAPTER I\' ackish watcsr to salt water. cbcl largely 1)y the zone of f STKUCTUKE This .sea, kr~ctwn as tht. Canadian Sl~ield,stoppeti lptly above the Palaeozoic The original uniform configuratiorl of the Palaeozoic tieposits of the Ottawa- Iley, and also east of Papi- St. Lawrence Lowland has been modified greatly by two major sets of faults. River, a scarp rises abovc. Of these, the principal set of faults, or in some places fault zones, has a general IIC faulting lies within thc east-southeast trend with a slight curve somewhat convex to the west of south. hcb north rise. with a gentle Towards the west of the basin the general direction of thcse faults is about ro1)ahly pc.11~tratccl farther south 60 degrees east. I'rogrcssively eastward they swing to more nearly J now tlrai~leclhy Gatinearl true east. The general pattern resel~~blcsslightly curvc\d radii stcmming not and North Natiorl Itivers. from a centre but from an elongated east-west mass to thc north of the western Champlain Sva ~cnetrated part of the hasin (Figure 3, in pocket). tcnac axis 11c.xt-i~to I,ake Most of the lesser set of faults dex-(,loped as relief to the stresses causecl Statc. by the primary faults. The whole pattern rc>flectsa torsion-tension movement to the north of east. Tlle faulting within the Canadiar~ part of the basin is almost entirely confined to the northern half, though a few minor faults extend southeast to the International Boundary. Ltoughly, the faulting forms the northern 15 replete. wit11 fossils and boundary of the present Palaeozoic formations, separating thctn from tl1c anti the unconsolidated Precambrian rocks. J modified by more recent 1 their long, winding tri- Due to the location of the faults the position of the Palzozoic betis relativc to the Precambrian rocks has four aspects on the northern margin of the basin. East of Papirleauville the Palaeozoic basin is separated from the highland> by the Grenville fault, with an abrupt rise of the Precambrian rocks on the upthrow side to the north. The exposures suggest only a small throw in this region because only the oldest Pal~ozoicrocks outcrop south of the fault. But the throw of the fault is probably considerably greater than is indicated by surface observations. A drill hole at Silica, Quebec, about 2 miles south of the present Precambrian scarp, revealed more than 500 feet of basal sandstone, which means either that the sand filled in an old channel or was depositetl in a sinking area. The abruptness of the Precambrian wall and its relatior1 to the downthrow side suggest an older fault, or perhaps subseql~entmovement along a former fault in the Precambrian. The second section extends from Papineauville to Hull, a distance of some 35 to 40 miles. In this section the two sets of faults cross into the northern edge of the Pal~ozoicarea, leaving a rim of the oldest Pal~ozoicsediments lying with a gentle monoclinic slope against the Prccambrian, north of the broken region. The third section extends roughly from Hull to a little west of Arnprior, approximately 35 miles. This section enters the narrowed area of the Pa- laeozoic sediments extending northwest up Ottawa Valley. The trend of the primary faults here parallels the direction of the valley. The Eardley fault on the northeast abruptly defines the limit of the Palaeozbic basin in that direction. On the southwest of the margin of the narrowed valley another fault of lesser throw separates the Palaeozoic sediments from the Precambrian rocks on that side. Between these two-faults are at least two others, perhaps have been usually detected more, that cut the Paleozoic sediments into long, narrow strips tilted towards formations. the northeast so that the older beds are brought up on their southwest sides. The exact age of the f In one place a Precambrian knob stands in the midst of the older formations place at one, two, or even D of Pa1l;eozoic rocks, brought to the surface on the upthrow side of one of these rocks are cut by the faults long, narrow blocks. post-Ordovician time. Th The fourth section is the northwest limit of the Paleozoic basin, which Devonian rocks enveloped narrows and is gradually lost in the Canadian Shield. Within this area are a pe~iodof faulting succet long, narrow grabens within which are the only Palzeozoi~rocks preserved. and Chaleur Bay region A1 The boundary faults of the grabens all have the same general trend as the at two periods, one at the primary faults of the entire basin. Lower Devonian. It is prc Lowland is related to the The main structural feature of the area is a large, down-dropped block that it is connected with t bounded by fault zones on the north, west, and south. The block extends eastward from the city of Ottawa. It is oblong, with its greatest dimension east-northeast, aad is so tilted that its maximum throw is at the west and south. About the centre of the block the gradual upward inclination eastward is interrupted by a slight break or further down-warping. From there eastward the upward inclination is resumed until the eastern extremity of the block almost regains its normal monoclinal position against the Precambrian rocks of the Beauharnois axis. The Gloucester fault, or fault zone, on the west and southwest margin of this block is the key fault of the central part of the area. The faulting on the north side of the block involves the 35 to 40-mile section of the basin in which the faulting along the northern margin of the lowland crosses Palaozoic sediments (Plate I11 B). This section of the fault system presents a peculiar tearing pattern and is part of the 'radial' fault pattern of the basin. On the north side of the longer faults of this margin of the block, secondary faults developed towards the northcast at an angle of 120 to 130 degrees to the longer faults and forming, within this marginal zone, numerous small tilted blocks, some of which are even upthrust. The long fault on the south and southeast of the block was clearly to relieve the tension along its northern margin, and the few secondary faults on the upthrow side where it bortlers the large down-faulted block afford relief to that more stable region. Almost all the faults ha\-e their largest displacement about midway of their length. The throw varies from zero to a maximum of approximately 1,800 feet, along the Gloucester fault, west of Russell where the Queenston shale is brought down to the level of the Oxford dolomite. It is to be notetl that a line joining the position of the maximum throw of the series of faults on the north of the large down-faulted block is practically parallel to the east-northeast fault forming the southern boundary of the block. This alinement of the position of maximum throw of each fault may be an expression of a buried Precambrian fault along which later movement has occurred. Along the linc of the Gloucebter fault the fault block to the east sinks at a nearly uniform rate. TIIF.older rocks of the upthrow side gradually rise until the Nepean sandstone is exposed about 2 miles north of South Gloucester, and then sink again, covered in turn by the March and Oxford. The dip of the faults has not been observed, but it is known to be steep around Ottawa where none of the numerous, closely placed wells crosses a fault plane. The faults, themselves, are concealed except in a few places where their positions are indicated 1,y clown-draggttl adjacent rocks. They kt least two others, perhaps have been rlsually detectctl by the juxtaposition of rocks of different k)c~isor larrow strips tilted towards formations. I> on their southwest sides. The exact age of the faulting cannot be established, nor whether it took lidst of the older formations place at one, two, or even more times. The fact that the youngest Ordovician pthrow side of one of these rocks are cut by the faults sllows that the latter must have developed during post-Ordovician time Thc preszncc on St. Helens Isle, Rlontreal, of Lower he Palaeozoic basin, whic11 Devonia.rl rocks enveloped by igneous rocks ant1 intruded by dyltes suggests eld. Within this area arct a period of faulting succeedirlg Lower Devonian deposition. In the Gaspe Pal~ozoi~rocks preserved. Chaleur Bay region Alcock (1935) has established that folding took place same general trend as thc at two one at tlie close of the Ordovician and one at the close of the Lower Devonian. It is probable that the faulting of the Ottawa-St. Lawrence Lowland is related to the disturbances of one or both of these periods and large, down-dropped block that it is connected with tlle northern Appalachian movements. ;outh. The block extends vith its greatest dimension throw is at the west and )ward inclination eastward arping. From there east- eastern extremity of th~ I against the Precambrian ult, or fault zone, on the J fault of the central part block involves the 35 to dong the northern margin I11 B). This section of and is part of the 'radial' onger faults of this margin :he northeast at an angle ling, within this marginal are even upthrust. The was clearly to relieve the lary faults on the upthrow afford relief to that more cement about midway of xim mum of approximately sell where the Queenston *mite. of the maximum throw of tulted block is practically mthern boundary of the maximum throw of each n fault along which later block to the east sinks at throw side gradually rise korth of South Gloucester, and Oxford. t it is known to be steep iy placed wells crosses a except in a few places d adjacent rocks. They heaped up by glacial action real for building purposes. Several outcrops of Ne for any purpose. CHAPTER V Oxford Dolomite. In dolomite is widely exposed beds. In the eastern part ECONOMIC GEOLOGY mainly of. dolomite, but it solidated deppsits. There No outstanding supply of economic minerals or metals has been found west but the stone is only 1~ within the area mapped. The Precambrian rocks to the north and west of the Gore tp., Que., is a quarry Pal~ozoiclowland have produced small, commercial quantities of mica, pyrite, Canadian Pacific north sl galena, molybdenite, celestite, graphite, apatite, feldspar, and quartz. In Iroquois, Ontario, are sevel recent years the discovery of brucite in limestone of the Grenville series, and part of the St. Lawrence c the utilization of dolomite beds in the same series, have afforded an abundant supplied some rough buildi source for the manufacture of basic refractory materials and metallic magne- In New York State to sium, and have opened up important industries. But the economic geology probable reason for the lac]. of the Precambrian rocks of these boundary areas is pertinent to the Ottawa- is the greater accessibility 1 St. Lawrence Lowland only to the degree to which it affects and will affect the increasing indllstrial life of this lowland. Rockcliffe Sandstone. ' and not very important r huilding stone and for flags St. Martin Limestone. limestone does not extend thin, impure, marginal dep

r 1 however, near Hawkesbur llie regloll ha& a large supply of good building stone. Seven types are limestone beds hav~been I rcadily available to any part of the basin: Grenville dolomite or limestone, Nepean sandstone, Oxford dolomite or limestone, Rockcliffe sandstone, St. Ottawa Limestone. T Martin limestone (to a limitetl degrrc), Ottawa limestone, and field stone. purposes -and in the city blocks, and residences. 'I Q~rarriedStone the Ottawa formation, co~ especiaIly suitable and h. Urenville l)olo?nite. 1,imestone and doloniite are among tile oldest of the In the upper half of the fc rocks in the Grenville sub-province of the Canatlian Shield. Though its supply. The latter beds : density makes it difficult to work, outcrops near towns on the Precambriau south bank of Ottawa Riy border of the basin have heen clrlarricd, particularly to supply material for scarp curves inland, cross foundations of buildings. past there have been a nu1 escarpment, but in recent .lTepean Sandstone. Thtb great tlurability, coarse grain, massive appear- city has grown. To the c aricc, and rust-mottlrd colour of the Nepean sandstone makc it a beautiful quarries, thc stone from and valuable stone for builcling purposes. It is perhaps more suitable for been shipped to neighbour large, massive architecture than for smaller buildings, though it has recently i~cenused for the lower story or even the foundations of private houses. Its To the south of the full ciign'ity, however, is revealed in the main Parliament Ruildings of the Rockland beds have s~pl I)ominion, standing on Parliament Hill. It has also heen used for many canal construction. other large government buildings in Ottawa. Altogether there are The supply for Ottawa has been taken for many years from outcropping Some have changed their J strata about TO miles west of the city, just north of Highway 15. The santl- Many of them are water-f stone forms a north-sonth ridge that crosses scvcral properties in Nepearl Stone fm Canal Con.? township. of the canals built to overt Near Mirabel, Quebec, about 8 or I) miles east of Lachute (Plate I1 A), Itivers. Along the Ottav arcx large areas piletl with loose masses of thick slabs of Nrpean sandston<. of Oxford and St. Afarti heaped up by glacial action. These are cut on the spot, and shipped to Mont- real for building purposes. Several outcrops of Nepean sandstone in the area have not yet been useti for any purpose. Oxford Dolomite. In the western part of the basin where the Oxfortl cjolomite is widely exposed the formation is thin and includes many impure beds. In the eastern part of the basin the formation is thicker and composed mainly of dolomite, but it is, for the most part, deeply covered by unconsolidated deposits. There are quarries, however, both in the east and in thc or mctals has been fount1 west but the stone is only locally used for building. On lot A, rge. 1, Lochaber o the north and west of the Gore tp., Que.. is a quarry the stone from which was uscd for culverts for the 1 quantities of mica, pyrite, Canadian Pacific north shore line between Rlontreal and Ottawa. Near feldspar, and quartz. In Iroquois, Ontario, are several quarries from which the rock was taken for that )f the Grenville series, and part of the St. Lawrence canal. Quarries in thr vicinity of Valleyfield have have afforded an abundant supplied some rough building stone. erials and metallic magne- In New York State to the south this rock is used more extensively. One But the economic geology probable reason for the lack of development of the dolomite within the lowland s pertinent to the Ottawa- is the greater accessibility of other material. t affects and will affect thc Rockclife Sandstone. The Rockcliffe sandstone is patchy in its occurrence, and hot very important economically. Nevertheless, it is used locally for building stone and for flagstones. St. Marcin Limestone. As has been shown, previously, the St. Martin limestone does not extend ovpr the western part of the basin, and is orily a thin, impure, marginal deposit in the central part. To the east and southeast, however, near Hawkesbury and along the St. Lawrence, the thicker, purer 4 stone. Sever1 types are limestone beds havz been quarried for building stone. Ile dolomite or limestone, Rockcliffe sandstone, St. Ottawa Limestone. The Ottawa linlestone is well adapted for building mestone, and field stone. purposes and in the city of Ottawa it has been used for churches, business blocks, and residences. The thick, pure limestone beds of the lower half of the Ottawa formation, comprising the Leray, Rockland, and Hull beds, art, especiaIly suitable and have been quarried extensively for building stone. e among the oldest of thr, In the upver half of the formation the Cobourg beds offer an almost limitless dian Shield. Though its supply. The latter beds are exposed largely in cliffs, such as those along the Bwns on the Precambrian south bank of Ottawa River from Rockcliffe to the west of Ottawa where the 'y to supply material for scarp curves inland, crossing west of the central section of the city. In the past there have been a number of quarries along the inland limb of this curved escarpment, but in recent years these old quarries have been tilled in as the 'e grain, massive appear- city Eias grown. To the east and southwest of Ottawa and in Hull are large tone make it a beautifuI " quarries, the stone from which has been used in Ottawa and Hull and has erhaps more suitable for been shipped to neighbouring towns. :s, though it has recently 1s of private houses. Its . To the south of the mapped area, the Mille Roches quarries in Leray- iiament Buildings of the Eockland beds have supplied building stone locally, and have been used ill Iso been used for many canal construction. Altogether there are scores of small quarries in the Ottawa limestone. - years from outcropping Some have changed their product to crushed stone; some have been abandoned. 9ighway 15. The sand- Many of them are water-filled, but they are still a potential resource. al properties in Nepean Stone for Canal Construction. Local stone was used in the construction of the canals built to overcome the rapids in Ottawa, St. Lawrence, and Rideau >f Lachute (Plate I1 A), Rivers. Along the Ottawa, at the Grenville and Carillon canals, great blocks bs of Nepean sandstone of Oxford and St. Martin limestone line the canal walls. In the series of St. Lawrence canals the type of rock used has depended mainly on the bedrock will again come illto prod through which the canals run. The canal banks are lined successively with new roads are constructed. Oxford limestone or dolomite, St. Martin limestoue, and the Leray-Rockland No place in the basin beds of the lower Ottawa limestone, the last obtained largely from the nearby ueeded. Mille Roches quarries. One large quarry, on lot A, con. X, Russell tp., now abandoned, supplied stone for both the Ottawa aud Cornwall canals. A large quarry north c Field Stone Cement Company. This c of very high calcium ca$)c Boulders of glacial origin are to be found, scattered sparpely over wide beds of the Ottawa formati areas or thickly congregated in others. Varied assortments takea from the More than 100 years : Kelds have been used in building farmhouscs, mills, and barns, but are now established' at Hull, thougl used mostly for foundations. The present plant has pro Selected Precambrian boulders, particularly those that are deeply coloured hands a number of times a are used locally in building residences, and are more widely used for ornamental A few other quarries chimneys and fireplaces. cement from time to time,

h number of large quarries produce crushed stone as a primary or secondary The Ottawa-St. Lawrc product: the quarry of the Canada Cement Conlpany north of Hull; Foster's i most of it is covrred wit quarry, southwest of' Ottawa; the quarry on the road running north from glacial origin is to be founc Eastview; the crushing plant of Devil's Garden at Rigaud; and the Mille to the ratreat of the glacie Roches quarries west of Cornwall are some that more recently have produced In addition, the invasion a crushed stone. Many small quarries are also producing it. and left irregularly placed h unique occurrence of boulders that are being brokei~up for crushed The sand of the basin stone is found on the north side of Rigaud Mountain, the Devil's Garden, in part coarser, less disint an area of many acres of amassed glacial boulders of considerable size, sorted the margins of the basin w to some degree. One theory of the origin of th(. accumlllation is that a sub- The gravels, too, were glacial stream rolled the boulders from the north up against the steep, northern ary streams, but although fault-face of Rigaud illountain. The deflected current was retarded, leaving in the main, was the result the boulders piled against the mountain face. A Montreal company has cut over which the glaciers n and crushed the boulders for various purposes, hut a considerable supply still from the rock beneath, evc remains. Where gravel is used for it North of the Mourltain road and 2 to 23 nlilcs west of Hull is an outcrop importance. When, how( of Grenville limestone that is crushed to make a sparkling white, pebbly action an economic factor material marketed for artificial stone, for a fine, white gravel used in walks, The Oxford formati01 and a variety of other domzstic products. basin. Some beds of dolt In addition, a number of quarries have been worked for railway ballast. limestone. Dolomite is a Perhaps the most outstanding of these is the large quarry in Oxford dolomite and magnesium carbonatc along the railway line bctween Oxford Mills and illerrickville, opened and more readily than the mat operated for the Canadian Pacific Railway. Another quarry in impure Gren- sium carbonate (magnesi ville limestone, northeast of Lachute, was used in the construction of bridge magnesium carbonate tal piers for the Canadian Pacific north shore line between Montreal and Ottawa. absorbed in the mixture. Numerous other smaller quarries are worked intermittently to supply local the expanding water crac needs. unately, can readily be , of the district. The construction of provincial, county, and township highways has made a large demand for crushed stone and gravels, and at least two score quarries This distinction betw operated for road metal have fallen more or less into disuse as the roads were should be considered in completed. The supply is there, however, and no doubt some of these quarries to frost action. 1 tded mainly on the bedrock will again cornc into production as c~sisting roads reyuirc improvement or I are lined srlccessively with new roads are constructed. 1 c, and the Leray-Rockland No place in the basin is far from a sourcc for cri~shetlsto~rc. when it is ed largely from the nearby rleedecl.

, now abandoned, supplied A large quarry uorth of Hull is now owned ant1 operated by the Canada Cement Company. This quarry, or series of quarries, produces a linlestone of very high calciun~carbonate content. The rock is mainly from the Hull attered sparaely over wide beds of the Ottawa formation. ~sortmentstakea from the More than 100 years ago the first hydraulic cement plant in Canada was s, and barns, but are now established at Hull, though the rock canie from the Ottawa side of the river. The present plant has prodvced for nearly 60 years, though it has changed hands a number of times and has bccll greatly enlarged during that period. se that are deeply coloured 7 widely used for ornamental A few other quarries have produced small quantities of limcxstone for cement from time to time, but they have closed down.

e as a primary or secondary The Ottawa-St. Lawrence basil1 ltas been subjected to glacial action, and ny north of Hull; Foster's most of it is cov,~red witli glacial debris. Every size of rock fragment of road running north from glacial origin is to be found, from silt and sand to large boulders. Subsequent at Rigaud; and the Mille to the ratreat of the glaciers the rivers have sorted the gravel in many places. ore recently have produced In addition, the invasion and retreat of the Champlain Sea deposited fine sand cing it. and left irregularly placed beach gravels, often of unsorted sizes. ng broken up for crushed The sand of the basin, therefore, is in part fine Champlain Sea sand, and ~tain,the Devil's Garden, in part coarser, less disintegrated sand of glacial origin, mostly piled around )f considerable size, sorted the margins of the basin within or at the edges of the Laurentian Hills. scumulation is that a sub- The gravels, too, were deposited in part by the Champlain Sea and tribut- against the steep, northern ary streams, but although their sorting was due to water action, their origin, rent was retarded, leaving in the main, was the result of glacial action. In large areas of exposed bedrock dontreal company has cut over which the glaciers moved the gravel would consist largely of material a considerable supply still from the rock beneath, even though it might contain many other constituents. Where gravel is used for itself, as on gravel roads, this factor is of no particular west of Hull is an outcrop importance. When, however, gravel is used for concrete exposed to frost L sparkling white, pebbly action an economic factor is involved. hite gravel used in walks, The Oxford formation is mostly dolomite, and covers a large area of the basin. Some beds of dolomite also occur in the lower 50 feet of the Ottawa rorked for railway ballast. limestone. Dolomite is a rock consisting of about equal proportions of calcium quarry in Oxford dolomite and magnesium carbonates. Upon exposure, the calcium carbonate dissolves Merrickville, opened and more readily than the magnesium carbonate leaving an outer lattice of magne- er quarry in impure Gren- sium carbonate (magneslte) crystals. When used in concrete the lattice of the construction of bridge magnesium carbonate takes up, in its interstices, more water than can be een Montreal and Ottawa. absorbed in the mixture. If placed near an outer surface reached by frost .mittently to supply local the expanding water cracks the concrete, forming a 'pop-out'. Such, unfort- unately, can readily be seen in many concrete roads and cement buildings . of the disti~ict. fnship highways has made st least two score quarries This distinction between pure limestone and dolomitic limestone in gravels o disuse as the roads were should be considered in preparing concrete for use in constru&ions exposed tubt some of theke quarries to frost action. . 40

Brick. The marine STONEFOR LIME making bricks, and brick! Lime is produced from the rocks of the Ottawa-St. Lawrence Lowland of the lowland. as lump lime, crushed quicklime, and slaked lime and is used for chemical, The red Queenston 5 metallurgical, constructional, and agricultural purposes. Thelargest plants, brick. It is quarried and however, are not within the area mapped, but farther up Ottawa Valley near Company, Limited, just \ the margin of the basin, at Carleton Place and within grabens at Fourth ChQte of the BonnechGre, and at Eganville. Within the map-area there are at least a dozen quarries that produce rock for lime in smaller quantites, as a secondary product. In the early days almost every farmer calcined limestone for lime. mortar, or agricultural purposes. The ruins of old limekilns dot the collntry side. The main urban pol ABRASIVESMATERIALS and water supplies are ti inland towns and village: At Silica, Quebec, about 16 miles east of Lachute and 23 miles east of the water into standpipe* St. Canute, there is a large quarry in the Nepean sandstone. The plant is wells, and is raised by n operated by the Canadian Carborundum Company, and the product is used hand pump. in the manufacture of carborundum and other abrasives. North of the area, 1 Drilling at this quarry showed that the sandstonp persisted to a depth from which adequate sup of at least 500 feet. parts of the area. No adequate survey 1 J~ISC~LLANEOUSUses of the entire basin, but s some informative data. Concrete Blocks. E'razer-Duntile Company, Limlted, operates a plant The typhoid epiden south of Carling Avenue and west of Ottawa. The stone is quarried from a drilling within the city 01 long ridge of the lower limestone beds of the Ottawa formation. It is cut for were put down. Six of sills and lintels, crushed for use in roofing or other construction, and processed sunk to depths of at leas for concrete blocks with air spaces for use in the interior of outer walls of Wells in the rural areas buildings. of these penetrate to any Ornamental S~OTLC.The limestone of the Leray beds, Ottawa formation, have not been kept. forms a long, low ridge across a number of lots of con. XII, Finch tp., Stormont The Ottawa limestol co. The stone is a very dark, pure, fine-grained limestone. It takes a high place depending upon th polish, and is sold commercially as a black marble for interior decoration. stone is not porous. TI It is shipped for this purpose to New York, Montreal, Toronto, Winnipeg, well water are obtained Vancouver, and other places. dolomite is relatively im Stone for Acid Towers. A number of plants near the large lumber mill3 layers allows free moven along Ottawa River quarry some of the purer limestone from the Ottawa It has also been sho formation for use in the acid towers of the sulphide pulp mills. table stands at different'] Ferrosilicon Alloys. At Beauharnois, Quebec, on St. Lawrence River, at several localities alon about 6 miles east of the eastern boundary of the map-area, St. Lawrence due either to escape alor Alloy and Metals Company, Limited, manufactures ferrosilicon products for if the faults are sealed a use in all grades of steel. Nepean sandstone with a very high percentage of catchment area of each 1: silica is the raw material. The principal source is at Melocheville, Quebec, about 3 miles east of the map-area, but material is also procured from Bucking- Within the large do ham and Perth, the latter just west of the area mapped. Russell, the main catchn and for some distance : Glass. Supplies of Nepenn sandstone for making glass and for use 111 block is covered by impel manufacturing steel have been taken from near the eastern part of the area. A deep well drilled in th~ The principal present sources are just east of Cascade Point, at the junction strata below that has m of Ottawa and St. Lawrence Rivers, and at Melochevi!le, Quebec. becomes too highly mine Brick. The marine clays of the Champlain Sea furnish material for making bricks, and brickyards, large and small, are to be seen in many parts va-St. Lawrence Lowland of the lowland. and is used for chemical, The red Queenston shale. from north of Russell is also used for making loses. The largest plants, brick. It is quarried and shipped to the plant of Ottawa Brick and Terracotta er up Ottawa Valley near Company, Limited, just west of Billings Bridge at Ottawa. I grabens at Fourth ChQtc tap-area there are at least :quantites, as a secondary WATER .Icined limestone for lime. limekilns dot the country

The main urban population is along Ottawa and St. Lawrence Rivers, and water supplies are taken from these rivers. A few of the smaller, more inland towns and villages make use of tributary streams and lakes, pumping ute arid 23 miles east of the water into standpipes. or large tanks. Elsewhere water is obtained from sandstone. The plant is wells, and is raised by windmill, electric or gasoline engine, force pump, or . and the product is used hand pump. Ives. North of the area, within the Precambrian Shield, are numerous lakes one persistetl to a cirptt~ from which adequate supplies of potable water may be obtained for northern parts of the area. No adequate survey has yet been made of the underground water resources of the entire basin, but such drilllng for water as has been done has provided some informative data. [mited, operates a plant The typhoid epidemic at Ottawa more than 30 years ago stimulated stone is quarried from a drilling within the city or in its immediate environs. More than eighty wel1,s , formation. It is cut for nstruction, and processed were put down. Six of them penetrated 1,000 feet or more, thirteen werc: ,nterior of outer wails of sunk to depths of at least 800 feet, and numerous others to 500 feet or more. Wells in the rural areas also have yielded some information, but not many of these penetrate to any great depth, and in many instances adequate records beds, Ottawa formation, have not been kept. XII, Finch tp., Stormont nestone. It takes a high The Ottawa limestone contains water, but the flow varies from place to place depending upon the continuity of cracks and joint planes, for the lime- 3 for interior decoration. stone is not porous. The largest and most continuous supplies of potable real, Toronto, Winnipeg, well water are obtained from the March formation. The cotrering of Oxford dolomite is relatively impervious, and the porosity of the March sandstone tr the large lumber mills layers allows free movement within the formation. ~estonefrom the Ottawa It has also been shown that the Gloucester fault is sealed, as the water- ulp mills. table stands at different levels on either side of it. On the other hand, drilling on St. Lawrence River, at several localities along the Montreal road has shown a scarcity of water, map-area, St. Lawrence due either to escape along the faults separating the irregular fault blocks, or, ferrosilicon products for if the faults are sealed as along the Gloucester fault, to the small size of the very high percentage of catchment area of each block. at Melocheville, Quebec, o procured from Bucking- Within the large down-dropped block that has its greatest throw west of Russell, the main catchment area is the exposed, porous or jointed rocks along ,ed. and for some distance south of Ottawa River. The southwest part of the ing glass and for use in block is covered by impermeable shales of the Billings and Carlsbad formations. eastern part of the area. A deep well drilled in this shale-covered area has shown that water within the Je Point, at the junction strata below that has migrated for a long distance from its catchment basin vi!le, Quebec. becomes too highly mineralized for domestic use. r

Comparative Anal?jses of

A number of mineral springs within the region have been used for medicinal purposes, and at one time provided quite an industry, but modern synthetically medicated waters have lessened the value of the natural saline springs. Health res'orts grew up around some groups of springs, such as Caledonia Springs and Constituents Carlsbad Springs (formerly Eastman Springs). Water was used from Victoria sulphur spring, near Green Creek, east of Ottawa; from Alfred, lot 10, con. VI, Alu inium ...... Alfred tp.; from Borthwick spring, east of Hawthorne, Gloucester tp.; from ~aaanese...... lot 9, con. VI, W. ( ?), Hawkesbury tp.; from Russell Lithia spring, near Calcium ...... Bourget; from Plantagenet springs; from Winchester springs; and from St. Strontium ...... Magnesium ...... Benoit spring. Another, rather weakly saline spring occurs at St: Eustache. Lithium ...... Two other springs occur west of the mapped area in the tongue of Palseozoic Potassium...... Sodium...... 2 rocks extending northwest up the Ottawa River Valley, namely Dominion Ammonium ...... spring, 2 miles from Pakenham, and Diamond Park spring on lot 26, con. XII, Carbon dioxide gas ...... Pakenham tp. The latter is radioactive, but loses its activity quickly because Hydrogen sulphlde gas...... of the small amount of radium dissolved in the water. Caledonia Springs, about 10 or 11 miles south of Hawkesbury, has been known since 1806. In early days it was not easily reached, but it is now on Radium emanations ...... the Canadian Pacific Railway line between Montreal and Ottawa. The source Dissolved radium ...... of the water is the Cobourg limestone beds of the upper part of the Ottawa formation. There are four springs, three of them, Saline, Sulphur, and Gas springs close together, the fourth, Cuncan spring, 2 miles distant. According I to Elworthy (1917, p. 24) these springs, the best known in Canada with the Carlsbad Springs, on exceptions of Banff Springs, Alberta, and Fairmont Springs, British Columbia, Ottawa to Montreal, is ab were the only ones that had been examined for radioactivity. springs in the neighbourhc been used for sulphur bat1 In addition, four artesian wells have been drilled at or near Caledonia from one ainother in deta Springs, one of which, the Artesian sulphur spring, penetrated 100 feet into Caledonia Springs. Five the rock and yielded water with sufficient hydrogen snlphide to be used for quantities of radium in sol sulphur baths. This artesian well and the four springs show some radium emanations and small quantities of radium in solution, but any radium eman- Both Caledonia Sprir ation in the gas at the mouth of the springs is immediately dispersed. Analyses summer accommodation. of the springs, made several times since they were known, have shown that Winchester Springs aI; the chemical content of the water varies over the years, the change supposedly due to variations in the rate of precipitation of certain of the constituent , villages, their centres prc minerals. A comparative table of the latest analysis made by Elworthy (1918) Alfred, and Hawkesbury of the four springs and the more important artesian well is as follows: poses. The more important Comparative Anolyses of Springs and Artesian Well at Caledonia Springs north half of the basin . springs appear to have 1 Iimestones the upper pbr Parts per million most water. The Caledc Constituents Artesian beds. In the Alfred sprin Saljne Sulphur Gas Duncan sulphur but considerable quanth spring spring sprlng spring spring --- -- springs issue from the s; chlorides with sbme bica Sulphuric acid ...... 2.1 3.3 2.1 3 '4 98.6 Bicarbonate acid ...... 930. 861 -0 925.0 1,200' 645 .O beds or alittle lower, is o Nitrous acid ...... Trace ...... 0.14 ...... 3.2 Winchester spring is mu Phosphoric acid ...... Trace I .O 1'2 ...... Metaboric acid ...... Trace Trace Trace Trace Trace Martin beds just above t Chlorine ...... 4,194.0 3,086.0 4.412- 5,137.5 1,418.5 Bromine ...... 10.0 14 3 2.4 10.0 4.8 Of those springs issi Iodine ...... 1 .6 2.5 0.6 1.5 Trace noteworthy. They issue Oxygen ...... 0.18 ...... 3.1 0.23 4.09 Silica ...... 15.0 17.9 17.1 10.9 21.7 The Borthwick spring, el Iron ...... 1 .2 Traces 0 ,G 1.3 1 .O predominate but with son Comparative Analysea of Springs and Artesian Well at Caledonia Springs Concluded ave been used for medicinal r, but modern synthetically ural saline springs. Health Parts per million 1 as Caledonia Springs and Constituents Art6sian Saljne Sulphur Gas Duncan sulphur ter was used from Victoria sprlng spring spring sprlng ~pr~ng .om Alfred, lot 10, con. VI, orne, Gloucester tp.; from Aluminium ...... 0.21 ...... 3.5 0.26 4.6 Manganese ...... 0.05 0.04 tussell Lithia spring, near Calcium ...... 41.0 39.8 70.8 43.5 27.7 ster springs; and from St. Strontium ...... 2.9 0.8 2.1 1.8 2.1 Magnesium ...... 143 .O 108 .O 137 .O 145.0 38.5 ng occurs at St: Eustache. Lithium ...... 2.4 1.8 4.7 17.2 1.6 n the tongue of Paleozoic Potassium...... 78.4 57.2 60.9 86 .O 37.5 Sodium ...... 2.691.4 2,030.6 2,808.94 3,339.3 1,076.2 Valley, namely Dominion Ammonium ...... 4.89 4.37 5.81 10.7 1.77 spring on lot 26, con. XII, Carbon dioxide gas ...... 40.5 61 .O 38 .5 48.7 30.4 ts activity quickly because Hydrogen sulphide gas...... 0.7 0.94 0.3 ...... 10.9 er. of Hawkesbury, has been Units reached, but it is now on and Ottawa. The source Radium emanations ...... I 7::6 1 73. 1 90. 1 53. I 56. Dissolved radium ...... 5 8.4 5 -6 1.7 upper part of the Ottawa SaIine, Sulphur, and Gas miles distant. According nown in Canada with the Carlsbad Springs, on the line of the Canadian National Railway from jprings, British Columbia, Ottawa to Montreal, is about 8 miles east of Ottawa. There are seveh saline lioactivity. springs in the neighbourhood, six of which belong to the Sanitorium and have been used for sulphur baths and medicinal drinking water. The springs differ Iled at or near Caledonia from one inother in details, but on the whole they reskmble the group at , penetrated 100 feet into n sblphide to be used for Caledonia Springs. Five of them show some radium emanations and minute prings show some radium quantities of radium in solution. )n, but any radium eman- Both Caledonia Springs and Carlsbad Springs still maintain a degree of ttely dispersed. Analyses summer accommodation. known, have shown that LPS, the change supposedly Winchester Springs and Plantagenet Springs have become small agricultural ertain of the constituent villages, their centres probably chosen because of the springs. Borthwick, made by Elworthy (1918) Alfred, and Hawkesbury springs have fallen into disuse for all practical pur- well is as follows: poses. The more important springs occur within the down-dropped block in the 11 at Caledonia Springs north half of the basin where there has been structural disturbance. The springs appear to have two sources -limestones and shale or clays. Of the million Iimestones the upper phrt of the Ottawa Ilmestone, the Cobourg beds, yields most water. The Caledonia springs, as mentioned above, come from these Artesian beds. In the Alfred spring, from the same source beds, chlorides predominate, i Duncan sulphur sprlng spring but considerable quantities of bicarbonates are present. The Plantagenet - springs issue from the same Cobourg beds, and contain a predominance of .1 3 '4 98.6 chlorides with sbme bicarbonates. The Hawkesbury spring, from the same .O 1,200' 645 .O beds oralittle lower, is of the same nature. The source of the water of the .14 ...... 3.2 Winchester spring is much lower stratigraphically, being from the thin St. .o 1'2 ...... e Trace Trace Martin beds just above the Rockcliffe formation. 5,137.5 1,418.5 4 10.0 4.8 Of those springs isshing from shale, the Carlsbad springs are the most 6 1.5 Trace They issue from the Carlsbad shales above the Billings shale. 1 0 23 4.09 noteworthy. 1 10 9 21.7 The Borthwick spring, east of Hawthorne, was of the type in which chlorides 6 1.3 1 .O predominate but with some bicarbonates. It has not been of commercial value. 44

Two small saline springs have been noted in Two Mountains county, Quebec, at St. Benoit and St. Eustache. The source of both is the clay over the Nepean sandstone. The St. Benoit spring carries mainly sodium chloride; the St. Eustache spring is only feebly saline.

OIL AND GAS 4 No wells drilled within the area mapped have shown more than a trace of oil, and that very rarely. A few fossils from the Eastview formation have displayed oil when split open, but oil is not an economic factor in the region. Gas has been reported from twelve wells, of which eleven were within the main down-dropped block. The gas has formed in isolated pockets in the black, bituminous Billings shale and in the Cobourg limestone beds of the Ottawa formation. The twelfth well is east of Cornwall and penetrates rocks of Chazy age. Both oil and gas occur only in isolated pockets, and have nowhere been 84266 found in commercial quantities. One well, just south of Ottawa in the Billings A. A bouldt formation, produced a flow of gas for 10 days. Another well, near the centre Quet of the fault block, produced sufficient gas for use in a private house. and

81893 Oxford dolomite weathering a n Two Mountains county, rce of both is the clay over ies mainly sodium chloride;

shown more than a trace e Eastview formation have nomic factor in the region. lich eleven were within the in isolated pockets in the murg limestone beds of the nwall and penetrates rocks ts, and have nowhere been th of Ottawa in the Billings A. A boulder hill of Nepean sal~dstone near Mirabel, :other well, near the centre Quebec. The loose rock is being cut in place a private house. and shipped to Montreal for building stone.

R Oxford dolo~nitecontaining cryptozoons and showing the characteristic weathering along joint planes. 95306

I. Ott;~w:~lil~leslo~~e :~l)or~t 250 fret above the t)asr. sho\virlg n n:ttor;rl profile of the

natural profile of the drag on tor Bay, Ottawa. I Adams, F. D. 1 (1884): On the Laurentian SJ Ami, H. M. (1882): Notes on an exposm River, Quebec; Ott The Utica Slate; ibid - Utica Slate Formatic (1883): Report on Geological Ottawa Field Nat. (1884): Notes on Ottawa Re1 (1885): Additional Notes on Field Nat. Club I1 (1887): The Great Ice Age a1 pp. 65-74, 81-88. (1888): On the Occurrence o Ottawa Nat. 2, pp Faulting in the Vicir Geology of the Gove On the Sequence of the Natural Gas C. (1892): Additional Notes 01 Ottawa Nat. 6, p~ - The Utica Terrane i (1893): Notes on Geology a County of Russel (1894): The Geology of Gal - Sazicava Sands and (1895): Report of the Geols DD. 167-169. A A (1899): Report of the Geolc pp. 218-223. 1 (1900): Geology of Some ( and Trans., 2nd : 1 (1902): Annual Report of Heavy layers of the Cobourg beds at thc top of the Ottawa formltior~,weathered by g1aci:rl Ottawa Nat. 15, action and forming the side of a buried channel underlying Sussex street, Ottawa, exposed during the excavation for the Customs Building in 1912-1913. - Brief Description o (1905): On the Geology of Antevs, E. 1 (1925): Retreat of the Last pp. 66-74, 95-97. huer, V. '(1930): Peat Bogs in Sout Bigsby, J. 1 (1824): A List of Mineral: Sci. 8, pp. 77-88.

1 Includes a part of the Ottawa-St CHAPTER VI

BIBLIOGRAPHY

Adams, F. D. (1884): On the Laurentian System; Ottawa Field Nat. Club I, Trs. 4, pp. 21-31. Ami, H. M. (1882): Notes on an exposure of the Potsdam formation at Buckingham Basin, Litvre River, Quebec; Ottawa Field Nat. Club I, Trs. 3, p. 39. The Utica Slate; ibid., pp. 61-66. - Utica Slate Formation in Canada (Abst.); Can. Nat. and Geol.; N.S. 10, p. 192. (1883): Report on Geological and Mineralogical Branch of Ottawa Field Naturalist Club; Ottawa Field Nat. Club I, Trs. 4, pp. 64-66. (1884): Notes on Ottawa Region; Ottawa Field Nat. Club 11, Trs. 5, pp. 118-121. (1885): Additional Notes on Geology and Pal~ontologyof Ottawa and Vicinity; Ottawa F~eldNat. Club 11, Trs. 6, pp. 251-259. (1887): The Great Ice Age and Subsequent Formations at Ottawa, Ontario; Ottawa Nat. I, pp. 65-74, 81-88. (1888): 0; the Occurrence of 'phosphatic nodules' in the Chazy Formation about Ottawa; Ottawa Nat. 2, pp. 45-46. Faulting in the Vicinity of Ottawa; ibid., p. 48. Geology of the Government Experimental Farm; ibid., pp. 71-72. On the Sequence of the Geological Formations about Ottawa, with Reference to the Natural Gas Question; Ibid., pp. 93-96. (1892): Additional Notes on the Geology and Paleontology of Ottawa and Its Environs; Ottawa Nat. 6, pp. 73-78. - The Utica Terrane in Canada; Can. Rec. Sci., 5, pp. 166-183 and 234-346. (1893): Notes on Geology and Paleontology of the Rockland Quarries and Vicinity in the County of Russell, Ontario, Canada; Ottawa Nat. 7, pp. 138-147. (1894): The Geology of Galetta, Ontario; Ottawa Nat. 8, p. 109. - Saxicava Sands and Gravels at Carp, Ontario; ibid., pp. 121-122. (1895): Report of the Geological Branch, bttawa Field ~a&ralistClub; Ottawa Nat. 9, pp. 167-169. (1899): Report of the Geological Branch, Ottawa Field Naturalist Club; Ottawa Nat. 13, pp. 218-223. I(1900): Geology of Some Cities in Eastern Canada (Ottawa); Roy. Soc., Canada, Proc. and Trans., 2nd ser. 6, sec. 4, pp. 129-138. mstion, weathered by glacial '(1902): Annual Report of the Geological Section of the Ottawa Field Naturalist Club; ying Sussex street, Ottawa, Ottawa Nat. 15, NO. 11, pp. 254-262. : in 1912-1913. - Brief Description of the Map of the Ottawa District; Ottawa Nat. 16, pp. 187-189. (1905): On the Geology of Carp (Ontario) and Environs; Ottawa Nat. 19, pp. 92-93. Antevs, E. 1 (1925): Retreat of the Last Ice-sheet in Eastern Canada; Geol. Surv., Canada, Mem. 146, pp. 66-74, 95-97. .4uer, V. '(1930): Peat Bogs in Southeastern Canada; Geol. Surv., Canada, Mem. 162, Index map. Bigsby, J. '(1824): A List of Minerals and Organic Remains Occurring in the Canadas; Amer. Jour.

Sci. 8, pp..- 77-88.

1 Ineludes a part of the Ottawa-St. Lawrence Lowland. Biesbv.- ". J. - Summary Report on (1825): Notice of a Cave containing Bones in Lanark, Upper Canada; Amer. Jour. Sci. 9, Quebec and Ontari, pp. 354-355. - Report on a Portion Bowman, A. "Eastern towns hi^ (1887): Testimony of Ottawa Clays and Gravels to the Expansion of the Gulf of St. Lawrence Montreal Sheet, PI and Canadian Lakes within the Human Period; Ottawa Nat. 1, pp. 149-161. - The Apatite-bearing Brummell, P. H. (1697): Notes on the Archsea H. pp. 121-124. 1 (1892): The Mineral Waters of Canada; Ottawa Nat. 6, pp. 160-167, 173-185. - Report (Summ.) on I Buchan, I. S. Quebec; Geol. Surv (1916): The Pleistocene of Montreal and Ottawa Valley from a Railway Carriage; Can. - (With remarks in pal Rec. Sci. 9, pp. 190-195. and Hastings Serie Chamberlin, T. C. (1898): Sands and Clays of t (1883): Geology of Wisconsin, Lower Silurian or Cambro-Silurian Age; Geol. Wisconsin, 1. - Report on Field Worl p. 154. and Carleton); Gel - Formations, Faults a Chapman, E. J. 1 (1864): A popular Exposition of the Minerals and Geology of Canada-Part V. Palaeozoic - Report on Field Wc Rocks of Canada; Can. Jour., N.S. 8, pp. 185-210. Geol. Surv., Canac (1864-1888): Exposition of the Minerals and ~eolo~~of Canada; First Edition - (1899): Report on Field Wc Third Edition. Geol. Surv., Canac The Mineral Resour* Cole, L. H. - (1911): Investigation of Reported Discovery of Tin Ore in the Vicinity of Arnprior, Ontario; (1900): Report on Field Wc Dept. of Mines, Canada, Mines Branch, Sum. Rept. 1910, pp. 93-94. Canada, Ann. Re1 (1923): Silica in Canada, Its Occurrence, Exploitation and Uses- Pt. I, Eastern Canada; - The Physical Featu) Dept. of Mines, Canada, Mines Branch, No. 555, pp. 45-48. Ottawa and St. Lr (1934): Sandstone at Hawkesbury, Ontario; Dept. of Mines, Mines Branch. Investigations 6, see. 4, pp. 99-12 of Mineral Resources and Mining Industry, 1932, pp. 7-9. (1901) : Ancient Channels of -- Report on the geolog Cole, L. H., and Carnochan, R. K. of Quebec and POI (1934):~, Silica Deposit near Gatineau Point. Quebec: De~t.of Mines. Canada. Mines Branch. 1n~esti'~ationsof Mineral and Mining 1ndus{ry, 1932, 3-6. Canada, Ann. Re1 (1902): Report on the Geol Coleman, A. P. of the City of Ott 1 (1901): Marine and Freshwater Beaches of Ontario; Geol. Soc., America, Bull. 12, pp. 129- pp. 1-51 (1899); E 146. (1903): Report on Field WI ' (1905): Glacial Lakes and Pleistocene Changes in the St. Lawrence Valley; Inter. Geol. Canada, Ann. Re] Cong. VIII, Rept. pp. 480-486. (1904): Report on the Geolc 1 (1932): An Interglacial Champlain Sea; Amer. Jour. Sci. 5, ser. 24, pp. 311-315. Rept. 14 (1901), 1 Craig, W. (1907): Report on the Geolc (1889): Contributions to the Geology and Palreontology of the Townships of Russell and west Quarter Shec Cambridge, in Russell, Ontario; Physiography and General Geology; Ottawa Counties of Ponti Nat. 2, pp. 136-139. pp. 1-71; Map Nc Dawson, Sir Wm. Ells, R. W., and Barlow, A. E. (1872): On the Post-pliocene of Canada, Ottawa River; Can. Nat. Geol., N.S. 6, pp. 252-253. (1895): The Physical Feat1 Dresser, J. A. St. Lawrence Ri- (1896): Petrographical Notes on some Archiean Rocks from Chelsea; Ottawa Nat. 10, 2nd ser. 1, sec. 4, pp. 129-133. Elworthy, R. T. Ells, R. W. (1918): Mineral Springs of (1893): The Laurentian of the Ottawa District; Geol. Sac. Amer., Bull. 4, pp. 349-360. Mineral Springs; (1894): Report on Field Work in Ottawa, Pontiac and Carleton Counties, Quebec and Foerste, A. F. Ontario; Geol. Surv., Canada, Ann. Rept. 7, pt. A, pp. 60-62. (1913): The Richmond For - Mica Deposits in the Laurentian of the Ottawa District; Geol. Soc. Amer.. Bull. 5, Sac. Amer., Bull. pp. 481-488. - Recent Deposits in the valley of the Ottawa River; Ottawa Nat. 8, pp. 104-107. Fraser, F. J. (1895): The Potsdam and Calciferous formations of Quebec and Eastern Ontario; Roy. (1931): Heavy Minerals in Sac., Canada, Proc. and Trans. 12, sec. 4, pp. 21-30. Surv., Canada, S - Report on Field Work in Ottawa and Argenteuil Counties, Quebec; Geol. Surv., Gauthier, H. Canada, Ann. Rept. 6 (1892), pt. A, pp. 37-40. (1917): Road Materials in (1896): Palreozoic Outliers in the Ottawa River Basin (followed by Ami's fossil list); Roy. Canada, Sum. R* Sac., Canada, Proc. and Trans., 2nd ser. 2, sec. 4, pp. 137-149. Giroux, N. J. - The Geology of the Ottawa and Parry Sound Railway; Ottawa Field Nat. 10. (1896): Report of Field Wc pp. 165-193. Canada, Ann. RI

r Giroux. N. J. Keele, J. i (1897): Re ort of Field Work in Eastern Ontario; Geol. Surv.. ~anida,Ann. Rept. 9 1 (1924): Preliminary Report 1 8896), pt. A, pp. 59-64. Ontario; Geol. Sur i.I Goldthwait. J. W. Keele, J.. and Cole, L. H. (1913): The Upper Marine Limit at Montreal, Covey Hill and Ottawa; Geol. Surv., Canada, 1 (1922): Structural Materials Inter. Geol. Congr. XII. Guide Bk. No. 3, .DD.- 119-126. and Lachine. Quek 1914): Marine Submergence at Montreal, Covey Hill and Rigaud Mountain; Geol. Surv., Keele, J., and Johnston. W. A. Canada, Sum. Rept. 1913, p. 211. (1913): The Superficial Dep (1926): Late Glacial Oscillations of Level in the St. Lawrence-Ottawa Valley (Abst.); Geol. XII, Guide Bk. 3, Soc., Amer., Bull. 37, No. 1, pp. 173-174; Pan Amer. Geol. 45, No. 2, p. 168. Kindle. E. M. Goranson. R. W. (1914): A Comparison of ti (1926): Calumet Island, Pontiac County, Quebec; Geol. Surv., Canada, Sum. Rept. 1925, Jour. Geol. 22, pp pt. C, pp. 107 and 115. (1918): An Ottawa Beach of Goudge. M. F. 1 (1919): The Climatic Inter] '(1933): Canadian Limestones for Building Purposes; Dept. of Mines, Canada, Mines Field Nat. 33, No Branch, No. 733, pp. 35-36, 72-74. Kindle, E. M.. and Burling, L. D '(1935): Limestones of Canada. Pt. 111, Quebec; Dept. of Mines, Canada, Mines Branch, (1915): Structural Relations NO. 755, pp. 13-19, 40-46, 58-68, 163-164. and St. Lawrence (1938): Limestones of Canada, Pt. IV, Ontario; Dept. of Mines, Canada, Mines Branch, NO. 781, pp. 12-16, 44-58, 77-82, 152-156, 180-183, 190-196. Logan, Sir Wm. E. 1 (1843): Preliminary Report Grant, Sir J. 1 (1845): Geol. Surv., Canad: (1864): The Geology of the Ottawa Valley; Caq. Nat. Geol., N.S. 1, pp. 419-426. 1 (1847): Geol. Surv., Canadr Harding, E.S. 1 (1852): Geol. Surv., Canad. (1907): The Treatment of Rheumatism at Caledonia Springs; Montreal Medical Journal. 1 (1857): Geol. Surv., Canad April. (1863): Geology of Canada Harding, W. D. to 1863. (1931): The Relations of the Grenville Sediments and the Potsdam Sandstone in Eastern 1 (1864): Atlas accompanyin Ontario; Amer. Miner. 16, p. 430. ?rTaddox. D. C. Harrington, B. J. 1 (1930): Deep Borings in C (1879): Report on the Minerals of Some of the Apatite-bearing Veins of Ottawa County, Sum. Rept. 192E Quebec; Geol. Surv., Canada, Rept. of Prog. 1877-78, pt. G. 1 (1931): Thickness of Ordo ' (1896): The Composition of Limestones and Dolomites from a Number of Geological Sum. Rept. 193C Horizons in Canada; Can. Rec. Sci. 6, pp. 27-32. McGerrigle, tl. W. Hunt, T. S. (1936): Lachute Map-area (1847): Mineral Springs; Geol. Surv., Canada, Rept. of Prog. 1845-46, pp. 119, 120. pt. C, pp. 41-62 (1865): On the Mineralogy of Eozoon canadense; Can. Nat. Geol., N.S. 2, pp. 120-128. Miller, A. H., French, C. 4.. W ' (1865): Contribution to the Chemistry of Natural Waters, No. 43, No. 47, and No. 65; (1931): Geophysical Surv Can. Nat. Geol., N.S. 2, pp. 172, 177, and 287. Canada, Mem. Ingall, E. D. Murray, A. ' (1926): Deep Borings in Ontario, Quebec, and Maritime Provinces; Geol. Surv., Canada, (1852): Report on the G Sum. Rept. 1924, pt. C, p. 241. Rideau Rivers; (1857): On the Geology Johnston, W. A. Madawaska Ri (1916): Late Pleistocene Oscillations of Sea-level in the Ottawa Valley; Geol. Surv., Canada. Mus. Bull. 24. Parks,I (1910): W. A. Preliminary Iiepc ' Sutton, Barrie, and Ottawa Areas, Ontario; Geol. Surv., Canada, Sum. Rept. 1915. p. 138. the Ottawa an, Pleistocene and Recent Deposits in the Vicinity of Ottawa, with a Description of Rept. 1910, pp the Soilh; Geol. Surv., Canada, Mem. 101; Map, Ottawa, Carleton, and Ottawa 1 (1912): Report on the Bui counties, Pub. No. 1662. Canada, Mines Deep Borings in Ontario, Quebec, and the Maritime Provinces; Geol. Surv., Canada, (1914): As above, No. 27 Sum. Rept. 1930, pt. D, pp. 67-84. Picher, R. H. Borings in Ontario, Quebec, and the Maritime Provinces; Geol. Surv.. Canada, (1917): Road Materials i Sum. Rept. 1931, pt. D, pp. 42-52. Sum. Rept. 19 Borings in Eastern Canada; Geol. Surv., Canada, Sum. Rept. 1932, pt. D, pp. 69-71 (1918): Road Materials i (1933); Geol. Surv., Canada, Sum. Rept. 1933, pt. D, pp. 155-156. rence River frc Kay, G. M. Mem. 106. (1939): Ottawa-BonnechPre Graben (Abst.); Geol. Soc., Amer., Bull. 50, p. 1915. Raymond (1942): Ottawa-BonnechPre Graben and Lake Ontario Homocline; Geol. Soc. Amer., Bull. (1911): Clay Sodules; (' 53, pp. 585-646. Keele. J. '(1924): Preliminary Report on Clay and Shale Deposits of Ontario - Clays of Eastern Ontario; Geol. Surv., Canada, Mem. 142. Chapter VII. pp. 50-70. Keele, J., and Cole, L. H. 1 and Ottawa; Geol. Surv., Canada, '(1922): Structural Materials along the St. Lawrence River, between Prescott, Ontario, 1 119-126. and Lachine, Quebec; Dept. of Mines, Canada, Mines Branch, No. 549. ld Rigaud Mountain; Geol. Surv., Keele, J., and Johnston, W. A. (1913): The Superficial Deposits near Ottawa; Geol. Surv., Canada, Inter. Geol. Congr. .ence-Ottawa Valley (Abst.); Geol. XII, Guide Bk. 3, pp. 126-135. n Amer. Geol. 45, No. 2, p. 168. Kindle, E. M. (1914): A Comparison of the Cambrian and Ordovician Ripple-marks found at Ottawa; Surv., Canada, Sum. Rept. 1925, Jour. Geol. 22, pp. 703-713. (1918): An Ottawa Beach of the Champlain Sea; Ottawa Nat. 32, pp. 83-86. 1 (1919): The Climatic Interpretation of Two Early Ordovician Mudcrark Horizons; Can. Dept. of Mines, Canada, Mines Field Nat. 33, NO. 5, p. 96. Kindle, E. M., and Burling, L. D. f Mines, Canada, Mines Branch, (1915): Structural Relations of the Precambrian and Paleozoic. Itocks North of the Ottawa and St. Lawrence Valleys; Geol. Surv., Canada, Mu,. Bull. 18. f Mines, Canada, Mines Branch, 183, 190-196. Logan. Sir Wm. E. '(1843): Preliminary Report, Geol. Surv., Canada, Rept. of Prog. 18q2 (1845): Geol. Surv., Canada, Rept. of Prog. 1845, pp. 28-33 bol., N.S. 1, pp. 419-426. (1847): Geol. Surv., Canada, Rept. of Prog. 1845-46, pp. 6-9, 47-67, 119-122. (1852): Geol. Surv., Canada, Rept. of Prog. 1851-52, pp. 6-20. ings; Montreal Medical Journal, (1857): Geol. Surv., Canada. Rept. of Prog. 1853-56, pp. 5-FL. 1 (1863): Geology of Canada: Geol. Surv., Canada, Rept. of Prog. from its commencen~ent to 1863. e Potsdam Sandstone in Eastern 1 (1864): Atlas accompanying Geology of Canada, Maps 1 and 2; Plate 3. Maddox, D. C. '(1930): Deep Borings in Ontario, Quebec, and Maritime Provinces; Geol. Surv., Canada, searing Veins of Ottawa County, Sum. Rept. 1928, pt. C, pp. 102-104. Ibid., Sum. Rept. 1929, pt. C, pp. 41-42. 177-78, pt. G. 1 (1931): Thickness of Ordovician Deposits in Ontario and Quehec; Geol. Surv., Canada, from a Number of Geological Sum. Rept. 1930, pt. D. pp. 49-57. McGerrigle, H. Mr. (1936): Lachute Map-area, Pt. 11, The Lowland Area; Que. Bur. of Mines, Ann. Rept., 'rog. 1845-46. pp. 119, 120. pt. C, pp. 41-62; Maps 408, East Half and Wrst Half. . Geol., N.S. 2, pp. 120-128. Miller, A. H., French, C. A,, Wilson, M. E. , No. 43, No. 47, and No. 65; (1931): Geophysical Survey of the Hull-(;lourester and Hazeldean Faults; Geol. Surv., Canada, Mem. 165, pp. 190-225. Murray. A. Provinces; Geol. Surv., Canada. (1852): Report on the Geology of the Region between the Ottawa, St. Lawrence, and Rideau Rivers; Geol. Surv., Canada, Rept. of Prog. 1851-52, pp. 57-91.

1 (1857): On the Geology and Topography of the Muskoka, Petawawa, BonnechBre, and Iwa Valley; Geol. Surv., Canada. Madawaska Rivers; Geol. Surv., Canada, Rept. of. Prog. 1853-56, pp. 94-98. Parka, W. A. iurv., Canada, Sum. Rept. 1915. '(1910): Preliminary Report on the Building and Ornamental Stones of Ontario South of the Ottawa and French Rivers; Dept. of Mines, Canada, Mines Branch, Sum. i Ottawa, with a Description of Rept. 1910, pp. 110-114. Ottawa, Carleton, and Ottawa 1 (1912): Report on the Building and Ornamental Stones of Canada -Quebec; Dept. of Mines, Canada, Mines Branch, No. 203, vol. 1, pp. 121, 126-138. Provinces; Geol. Surv., Canada. (1914): As above, No. 279, vol. 3, pp. 121. rovinces; Geol. Surv.. Canada, Picher, R. H. (1917): Road Materials in Soulanges and Vaudreuil Counties, Quebec; Geol. Surv.. Canada, Sum. Rept. 1916, pp. 201-206. tm. Rept. 1932, pt. D, pp. 69-71 )t. D, pp. 155-156. (1918): Road Materials in a Portion of Vaudreuil County, Quebec, and along the St. Law- rence River from the Quebec Boundary to Cardinal, Ontario; Geol. Surv.. Canada. Mem. 106. ter., Bull. 50, p. 1915. ocline; Geol. Soc. Amer., Bull. Raymond (1911): Clay Nodules; Ottawa Nat. 24, pp. 147-148. Reinecke, L. : ' 1 (1915): Road Materials in Ontario; Geol. Surv., Canada, Sum. Rept. 1914, pp. 88-90. (1924) Arnprior-Quyon and Mem. 136; Map, PI (1916): Road Materials in Ontario and Quebec; Geol. Surv., ~aAda,sum.. Rept. 1915, pp. 147-155. - ' Ontario's Lead Mine; (1917): Road Material Surveys in 1915; Geol. Surv., Canada, Mem. 99; Map, Pub. No. 1665, 1 11925):.- , The Grenville Precan and Map 168A, Pub. No. 1653. (1931): Ripple-marks in the No. 14, pp. 347-34F Retty. J. A. - Ripple-marks near P '(1933): Reconnaissance along the Coulonge and Black Rivers, Pontiac County. Quebec; pp. 25-27. Que. Bur. Mines, 1932, pt. D, pp. 99-103. (1932): 'Samson's Boulder St Satterly, J., and Elworthy, R. T. Nat. 46, pp. 177-17 (1917): Mineral Springs of Canada, Pt. I - The Radioactivity of some Canadian Mineral - The Mammillary Mo Springs; Dept. of Mines, Canada, Mines Branch, Bull. 16, Pub. No. 435. Wilson, W. J. Selwyn, A. R. C. (1898): Notes on the Pleisto (1882): On the Geology of the Ottawa Palceozoic Basin; Ottawa Field Nat. Club I, Trs. Nat. 11, pp. 209-2: No. 3, pp. 34-39. Wright. J. F. Stewart, John (1923): Brockville and Mall (1887): The Development of the Mines of the Ottawa Region;- Ottawa Field Nat. Club 111. Pub. No. 1964. pp. 33-39: '(1888): Notes on Geological work of the Summer 1887; Ottawa Nat. I, pp. 170-171. Vennor, H. G. Ami. H. M. '(1875): Notes on Some of the Galena or Sulphuret of Lead Deposits Connected with the (1883): Notes on Triarthrus Laurentian Rocks of Ontario; Can. Nat., N.S. 7, pp. 455-462. - (1884): List of Fossils from (1876): Explorations and Surveys in the Rear Portions of Frontenac and Lanark Counties. 54-62. together with Notes on' Some of the Econolnic Minerals of Ontario; Geol. Surv., (1887): Notes on the Precis Canada, Rept. of Prog. 1874-75, pp. 105-165. Ottawa Nat. I, pp ' (1877): Archiean of Canada; Amer. Jour. Sci. (3) 14, pp. 313-316. - On the Occurrence '(1878): Geol. Surv., Canada, Rept. of Prog. 1876-77, pp. 244-264, 277. tario; Can. Rec. E Whittaker, E. J. (1888): On Utica Fossils frc (1922): Bottom Deposits of McKay Lake, Ottawa; Roy. Soc., Canada. Proc. and Trans., (1889): Contributions to th 3rd. ser. 16, sec. 4, pp. 141-156. Cambridge, in R1 (1895): Fossil Insects from Wilson, A. E. 190-191. (1932): Notes on the Pamelia Member of the Black River Formation of the Ottawa Valley; Amer. Jour. Sci. 24, pp. 135.146. 1 (1896): Notes on Canadian (With Ells, R. W.) (1937): Erosional Intervals Indicated by Contacts in the Vicinity of Ottawa. Ontario; - Roy. Soc., Canada, Proc. and Trans., 3rd ser. 31, sec. 4, pp. 45-60. Format ions and Proc. and Trans. Wilson, A. E., Stewart, J. S., and Caley, J. F. (1897): Contribution to th (1941): Sedimentary Basins of Ontario, possible Sources of Oil and Gas; Roy. SOC..Canada, Valley; Ottawa ? Proc. and Trans., 3rd ser. 35, sec. 4, pp. 167-185. (1899): On Some Trenton berland County Wilson. 31. E. (1914): Southeastern Portion of Buckingham Map-area, Quebec; Geol. Surv., Canada. --- ,1901): Preliminary Lists Sum. Rept. 1913, pp. 196-207. Comprised in thc of Quebec and , (1915): Northern Portion of the Buckingham Map-area, Quebec; Geol. Surv., Canada, Rept. 12, pp. 49 Sum. Rept. 1914, p. 94. - Lists of Fossils 0 (1916): Southwestern Portion of the Buckingham Map-area, Quebec; Geol. Surv.. Canada. Pertaining to tl Sum. Rept. 1915, pp. 156.162. Geol. Surv., Can (1917): Grenville District, Argenteuil County, Part of Amherst Township. Labelle County, '1904): Prelimipary Lists a Quebec; Geol. Surv., Canada, Sum. Rept. 1916, pp. 208-219. cene Formations (1918): The Amprior-Quyon District, Ontario and Quebec; GeoJ. Surv., Canada, Sum. Geol. Surv., Car Rept. 1917, pt. E, pp. 42-43. (1920): Buckingham Map-area, Map, Pub. No. 1691. Bsssler, R. S. 1 (1935): Classification of I! - - Mineral Deposits in the Ottawa \-alley; Geol Surv., Canada, Sum. Rept. 1919. pt E, pp. 19-44. Bather, F. A. -- JIolybdenite in the 1,onrer Ottawa Valley; Can. Inst. Min. and Met., Monthly 1 (1900): Treatise on Zool., null. 102, pp 749-754. 1 (1908): Studies in Edrioa (19'21). Ibid., Can. Min. Inst., Trs. 23, pp. 419-425. 1 (1913) : Caradocian Cystic - 452-467. The Relationships of the Palaeozoic to the Precambrian along the Southern Border The Trenton Crir of the Laurentian Highlands in Southeastern Ontario and the adjacent Portions cott); Geol. Su: of Queber: Roy Soc., Canada, Proc. and Trans., 3rd ser. 14, sec. 4, pp. 15-24. 1 Includes some forms from the Sum. Rept. 1914, pp. 88-90. (1924): Arnprior-Quyou and hlaniwaki Areas, Ontario and Quebec, Geol. Surv., Canada. urv., Canada, Sum. Rept. 1915, Men]. 136; Map, Pub. No. 1739. - Ontario's Lead Mine; Can. Min. Jour. 45, Nos. 20 and 21, pp. 477-478 and 501-502. la, Mem. 99; Map. Pub. NO. 1665. (1925): The Grenville Precambrian Subprovince; Jour. Geol. 33, No. 4, pp. 389-407. -(1931): Ripple-marks in the Lower Palreozoics of Ottawa Valley; Can. Min. Jour. 62, No. 14, pp. 347-348. tivers, Pontiac County, Quebec; ---- Ripple-marks near Perth, Lanark County, Ontario; Can. Field Nat. 45. No. 2. pp. 25-27. (1932): 'Samson's Boulder Stone' an Erratic near Perth, Lanark County, Ontario; Ottawa Nat. 46, pp. 177-178. tivity of some Canadian Mineral The Mammillary Mounds of the Bonnech6re Valley; Ottawa Nat. 46, pp. 32-33. h, Bull. 16, Pub. No. 435. Wilson, W. J. (1898): Notes on the Pleistocene Geology of a Few l'laces in the Ottawa Valley; Ottawa Ottawa Field Nat. Club I, Trs. Nat. 11, pp. 209-220. Wright, J. F. (1923): Brockville and Malloryto\vr~ Map-area; Grol Surv.. Canada, Mem. 1%; Map. ion; Ottawa Field Nat. Club 111, Pul) No. 1964. ttawa Nat. I, pp. 170-171.

Ami, H. M. f.d Deposits Connected with the Notes on Triarthrus spinosus Billings; Ottawa Field Nat. Club I, Trs. 4, pp. 88-89. .. pp. 455-462. (1883): List of Fossils from Ottawa and Vicinity; Ottawa Field Nat. Club 11, Trs. 5, pp. 'rontenac and Lanark Counties, (I=): [inerals of Ontario; Geol. Surv., 54-62.- - Notes on the Precise Geolo,oical Horizon of Siphonotreta scotia Davidson (Utica); Ottawa Nat. I, pp. 121-126. On the Occurrence of Scolithus in Rocks of Chazy Formation about Ottawa, On- tario; Can. Rec. Sci. 2, pp. 304-306. On Utica Fossils from Rideau, Ottawa, Ottawa Nat. I, pp. 165-169. ;oc., Canada. Proc. and Trans., Contributions to the Geology and Palzontology of the Townships of Russell and Cambridge, in Russell, Ontario; Palreontology; Ottawa Nat. 2, pp. 139-140. Fossil Insects from the Leda Clays of Ottawa and Vicinity; Ottawa Nat. 9, pp. 'ormation of the Ottawa Valley; 190-191. Notes on Canadian Fossil Bryozoa; Can. Rec. Sci. 6, pp. 222-229. Vicinity of Ottawa, Ontario; (With Ells, R. W.) Fossil Organic Remains comprised in the Various Geological . sec. 4, pp. 45-60. Formations and Outliers of the Ottawa Palzozoic Basin; Roy. Sac., Canada, Proc. and Trans., 2nd. ser. 2, sec. 4, pp. 151-158. Contribution to the Palaeontology of the Post-Pliocene Deposits of the Ottawa )il and Gas; Roy. SOC.,Canada, Valley; Ottawa Nat. 11, pp. 20-26. On Some Trenton (Ordovician) Fossils from the Light Grey Limestones of Cum- berland County of Russell, Ontario; Ottawa Nat. 13, pp. 238-240. Juebec; Geol. Surv., Canada. Preliminary Lists of Organic Remains Occurring in Various Geological Horizons Comprised in the Map of Ottawa District, Including Formations in the Provinces 2uebec; Geol. Surv., Canada, of Quebec and Ontario, along the Ottawa River; Geol. Surv., Canada. Ann. Rept. 12, pp. 49-77. Quebec; Geol. Surv., Canada, Lists of Fossils Obtained from the Several Formations along the Ottawa River Pertaining to the Report of Sheet No. 121 (Grenville), Quebec and Ontario; Geol. Surv., Canada, Ann. Rept. 12, pt. J, pp. 139-143. rst Township, Labelle County, p. 208-219. Prelimipary Lists of Fossil Organic Remains from the Potsdam-Utica and Pleisto- cene Formations Comprised within the Perth sheet (No. 119) in eastern Ontario; ; Geol. Surv., Canada, Sum. Geol. Surv., Canada, Ann. Rept. 14, pt. J, pp. 80-89. Bassler. R. S. -.. Cansda, Sum. Rept. 1919. '(1935): Classification of Edrioasteroidea; Smith. Inst. 93, No. 8, p. 4. Bather. F. A. 1st. Min. and Met.. Monthly 1 (1900): Treatise on Zool., Pt. 3, Echipoderms, pp. 200, 209, 210. 1 (1908): Studies in Edrioaster, 111; Geol. Mag., dec. 5, vol. 5, pp. 543-550. 1 (1913): Caradocian Cystidea from Girvan; Edinburgh. Trans. Roy. Soc. 49, pt. 2. pp. 397. an along the Southern Border 452-467. rio and the adjacent Portions The Trenton Crinoid, Oltawacrinus, W. R. Billings, and Note on Meroesinus (Wel- rd ser. 14, sec. 4, pp. 15-24. cott); Geol. Surv., Canada. Mus. Bull. l, No. l, pp. 1-10. 1 Includes some forms from the Ottawa-St. Lawrence Lowland. Rather, F. A. (1883): Notes on and Descl '(1928): Dendroeystis in North America; Geol. Surv., Canada, Bull. 49, pp. 5-8. Field Nat. Club I

Billings, E. (1885): Two New Species 1 (1854): On Some New Genera and Species of Cystidea from the Trenton 1;imestone; Can. Trs. 6, pp. 248-25 Jour. 2, pp.- - 215-218, 250-253, 268-274. - Additionsl~oteson (1857): Fossils of the Potsdam Sandstone and Footprints on the Rock at Beauharnois; Field Nat. Club I Can. Nat. Geol. 1, pp. 32-39. - Report of the Pal: On Some Characteristic Fossils of the Lower Silurian Rocks of Canada; Ibid., Ottawa Field Na pp. 39-47. (1887): A New Genus and On the Crinoidea or Stone Lilies of the Trenton Limestone, with the Description Notes on a Larp of a New Species; ibid., pp. 48-57. 49-51. On the Fossil Corals of the Lower Filurian Rocks of Canada; Ibid., pp. 116-128. Carpenter. W. D.

On Some of the Lower Silurian Fossils of Canada; ibid., pp. 203-208. f (1865): Notes on the Struct Description of Fossils Occurring in the Silurian Rocks of Canada; ibid., pp. 312320,. pp. 111-120. On the Tertiary (Quaternary) Rocks of Canada, with Some .Account of Their Chapman, E. J. Fossils; ibid., pp. 321-346. (1860): On a New Species - New Species of Fossils from the Silurian Rocks of Canada; Geol. Surv.. Canada. Can. Jour., N.S. Rept. of Prog. 1853-56, pp. 256-345. 1 (1861-1863): A pbpular Ex --- On the Genera of Fossil Cephalopods Occurring in Canada; Can. Nat. Geol. 2, Remarks on Org pp. 135-138. Jour., N.S. 6, pl (1858): Geol. Surv., Canada, Rept. of Prog. 1857, pp. 147-162, 179-192. (1877): On the Probable P. - On the Cystidea of the Lower Silurian Rocks of Canada; Geol. Surv., Canada, Climactiehnites; , Can. Org. Rem. dec. 3, pp. 9-74. Clarke, J. M. --- On the Asteriadae of the Lower Silurian Rocks of Canada; ibid., pp. 75-85. f (1892): Brachiopoda; Geol - New Genera and Species of Fossils from the Silurian and Devonian Formations of (1901): New Agelnrrinites Canada; Can. Nat. Geol. 3, pp. 432-444. (1859): On the Crinoideae of the Lower Silurian Rocks of Canada; Geol. Surv.. Canada, Cox, I. Can. Org. Rem. dec. 4, pp. 1-72. (1936): Revision of the (; pp. 7-11. - Description of a New Genus of Brachiopod and on the Genus Cyrtodonta; Can. Nat. Geol. 4, pp. 301-303. Dana, J. U. Fossils of the Calciferous Sandrock (includes those of deposit of white limestone at (1871): On the Supposed Mingan supposed to belong to the formation); ibid., pp. 345-367. Hist. 4, ser. 7, 1 Description of Some New Species of Trilobites from the Lower and Middle Silurian (1872): Ibid.; Can. Nat. 1 Rocks of Canada; ibid., pp. 367-383. Possils of the Chazy Limestone with Description of New Species; ibid., pp. 426-470. Ilavidson, T., and King, W. - Atrypa hemiplicata; Can. Jour., N.S. 4, p. 316. 1 (1874): On the Trimerelli, (1860): Additional Note on the Potsdam Fossils; Amer. Jour. Sci. (2) 30, pp. 242-243, Quart. Jour. Ga 337-338. I)awson, Sir Wm. - Description of Some New Species of Fossils from Lower and Middle Silurian Rocks On the Fossils of of Canada; Can. Nat. Geol. 5, pp. 49-69, 161-177. 1 (1864): 1 (1865): On Certain Orga (1861): On the Trark of an Sni1n:tl Lately Found in the Potsdarn Formation; Amer. Jour. Geol., N.S. 2, 1 Sci., 2nd ser. 31, pp. 17-23. --- 1 (1868): The Evidence of Astylospongia parvula Bill~nys;Itept. on Geology of Vermont 2, p. 956. Canada; Can. (1863): Description of a New Species of Rarpes from the Trenton 1,imestone. Ottawa; Can. Nat. Geol. 8, pp. 36-38. (1877): Xotes on a Fos~ - No. 6, pp. 340 Geology of Canada; Geol. Surv., Canada. (1888): Geological Histo - -I (1865): Palreozoic Fossils, vol. 1 (Adv. sheets 1862); Geol. Surv., Canada. (1889): Note on Holantc: - Notice of Some New Genera and Specirs of Paleozoic Fossils; Can. Nat. Geol., pp. 287-289. N.S. 2, pp. 325-432. - Note on an Ech --- Notes on Some of the More Remarkable Genera of Silurian and Devonian Fossils; Pleistocene (I Can. Nat. Geol., N.S. 2, pp. 184-198. 1 (1890): On Burrows an (1869): On the Structure of the Crinoidca, Cystidea, and Blastoidea; Can. Nat. 4, pp 277- Markings; 1.0 293, 426-433; Amer. Jodr. Sci. 2, ser. 48, pp. 69-82. (1891): Notice of ahovt (1870): Ibid. (Continued); Can. Nat. Geol. 5. DD... 180-198; Amer. Jour. Sci. 49. -PP. - 51-58 - Notes on Some Specimens of Lower Silurian Trilobites; London Quart. .Jour. Geol. Delo, D. M. Soc. 26, pp. 479-486; Notice; Can. Nat. Geol., N.S. 5, pp. 90-92. 1 (1940) : I'hrrcopid Trilol (1872): On the Genus Obolellina; Can. Nat., N.S. 6, pp. 326-333. 111 and 132. (1876): On openings in Arms of Actinor7inus; Amer. Jour. Sci. (3) 11, pp. 176-178. I)onald, J. Billings, W. R. 1 (1899): Ileu~arks011 t'lc (1881): Notes on Two Species and One Genus of Possils from the Trenton Tjirrrr.sto~re. of British Sp Ottawa: Ottawa Field Nat. Clul, I, Trs. 2, pp. 34-35. da, l

Canada; ibid., pp. 75-85. Clarke, J. M. 1 (1892): Brach~o~oda,Geol. Surv., State New YorL, l'alieontology \ 111, pis I and 11. an and Devonian Formations of 1 (1901) New .4gelorr1rrttes; Ne11 York State hfus Bull 49, p 191 Canada; Geol. Surv.. Canada, Cox, I. (1936): ltevision of the Germs ('crlopn7rio I%illings;1)ept. of Mines. Canada, Mus. Bull. 80, In the Genus Cyrtodonta; Can pp. 7-11. Dana, J. D. of deposit of white limestone at (1871): On the Supposed Legs of the Trilobite .4xnphr~s plnt,ycrphnltcs; .inn. Mag. Nat. lid., pp. 345-367. Hist. 4, ser. 7, pp. 366-368. I the Lower and Middle Silurian (1872): Ibid.; Can. Nat. Geol.. N.S 6, pp. 348.350 New Species; ibid., pp. 426-470. Davidson, T., and King, n'. 1 (1874): On the Trimerellidae, .i l'ala3ozoir Fau~ilyof 1'illliol)rnnrhs or Hr;~c.l~iopoda;1,ondon .four. Sci. (2) 30, pp. 242-243, Quart. .Tour. Geol. Soc. 30, pp. 162 and 165.

Bwer and Middle Silurian Rocks I)awson, Sir Wni. 1 (1864):. . On the Fossils of the Genus Rusophycus; Can. Nat. Geol., N.S. 1, pp. 363-367 ~tsdamFormation; Amer. Jour. 1 (1865): On Certain Organic Remains in the Laurentian 1,imestones of Canada; Can. Nat. Geol.. N.S. 2, -pp. - 99-111, 127. Vermont 2. p. 956. 1 (1968): The Evidence of Fossil Plants as to the Climate of the Post-pliocene Period in Canada; Can. Nat. Geol., N.S. pp. e Trenton Limestone. Ottawa; 3, 69-76. (1877): Notes on a Fossil Seal from the Leda Clay of the Ottawa Valley; Can. Nat. 8. No. 6, pp. 340-341. Geological History of Plants, pp. 227-233. wv., Canada. (1888):. , - Note on Ralanus Humeri in the Pleistocene at Hiviere Beaudette; Can. Rec. Sci. 3. ozoic Fossils; Can. Nat. Geol., (1889): .OD.. 287-289. - Note on an Echinoderm Collected by Dr. Ami at Besserers, Ottawa River, in the Silurian and Devonian Fossils; Pleistocene (Leda Clay); Ottawa Nat. 13, pp. 201-202. On Burrows and Tracks of Tnvertebrate Animals in Palaeozoic Rocks and Other 'astoidea; Can. Nat. 4, pp. 277- 1 (18%): !. Markings; London Quart. Jour. Geol. Soc. 46, pp. 595-618. Notice of above; Can. Rec. Sci. 4, pp. 234-23.5. bmer. Jour. Sci. 49, pp. 51-58. (1891): tes; London Quart. Jour. Geol. Delo, D. M. 3. 5. pp. 90-92. 1 (1940): Phacopid Trilohites of North America; Geol. Soc. Amer., Spec.. Pap. 29, pp. 110- 333. 111 and 132. ci. (3) 11, pp. 176-178. Donald, J. 1 (1899): Itelnarks on the Genera Ectomuriu Koken and liormotoma Salter, with Descriptions from the Trenton Limestone. of nritish Species; London Quart. Jour. Geol. 55, pp. 253-255, 262, 263. -35. Foerste, A. F. ' (1914): Notes on the Lorraine Faunas of New York and the Proviuce of Quebec; Deniaon Jaekel. 0. Univ., Bull. 17, pp. 247-339. 1 (1899) : Stamm. Pelmatozoa Notes on the Agelacrinidae and Lepidocystinae, with Description of Thresherodiscus Jones, T. R. and Brockocystites; ibid., pp. 399-474. 1 (1858): Notes on Pal=ozoic i1916): Comarocystites and Caryocrinus; Ottawa Nat. 30, pp. 69-79, 85 03, 101-111. - 1 On the Palreozoic 1 - ' Notes on Cincinnatian Fossils (Cystid); Denison Univ. Sci. Lab., Bull. 18, pp. 340- Om. Rem. dec. 3, 341. 1 (1891): On some Ostracoda ' Upper Ordovician Faunas of Ontario and Quebec; Geol. Surv., Canada, Mem. 83. From the Cambrc Micro-Pal., pt. 11 (1919): Notes on Zsotelus, Acrolichas, Calymene, and Bncrinurus; Denison Univ. Bull. 19.

DD..a 65-82. Kindle. E. M. (1920): Kimmswick arid Plattin Limestones of Northeastern Missouri; Denison Univ. Sci. (1917): Recent and Fossil 1 Lab. 19, PI. 22, fig. 23. and 44, and Pls. 4 - The Generic Relations of the American Ordovician Lichadilae; Amer. Jour. Sci. 4, (1926): A comparison of Rt ser. 49, pp. 26-50. Habitats; Can. F, (1922): Distribution of the Ottawa Trenton Echinoderm Faunas; Can. Nat. 36. No. 5. (1928): A Crustacean New t pp. 84-86. pp. 211-212. 9 Upper Ordovician Faunas of Ontario and Quebec; Geol Surv.. Canada, Mem. 138. - Notes on American Pal=ozoic Cephalnpods; Denison Univ. Sci. Lab., Bull. 20, Knight, J. Brookes pp. 232-234. 1 (1941): Palreozoic Gastropo ' (1930): The Actinoceroids of East Central North America; Denison Univ. Sci. Lab., Bull. Lambe, L. M. 25, pp. 248-249, 292-293. (1897): Description of a ' (1932): Black River and other Cephalopods from Minnesota, Wisconsin, Michigan, and Can. Rec. Sci. 7, Ontario, Pt. 1; Denison Univ. Sci. Lab. 27. (1899): A Revision of the G (1933): Ibid., Pt. IT; Denison Univ. Pci. Lab. 28. poraria, Perforatr 1bid.- The Madrel Foord, A. H. 1 (1900) : ' (1883): On the M~nticuli~oridaeof the Chazy, Black River, and Trenton Formations, Logan. Sir Wm. E. with Descriptions of Ten New Species; Geol. Surv., Canada, Con. Micro-Pa].. (1852): On the Footprints ( pp. 1-26. Jour. Geol. 8, pp Grant. Sir J. (1861): On the Track of an (1880): Cystidearl Life; Ottawa Field Nat. Club I, Trs. 1, pp. 26-31. pp. 279-285; Am1 (1881): Description of a New Species of Porocrinus; Ottawa Field Nat. Club I. Trs. 2, (1889): Ibid., republished: pp. 42-44. Miller, A. K. Haekel, E. '(1943): OzarkianSpec. Pap. and 49, CRI p. (1896): Die Amphorideen und Cystoideen, pp. 41-42, 44-45, 69-70, 105-107, 118, 150, PI. 1, figs. 4-4c; PI. 2, figs. 15 and 16; PI. 3, figs. 29, 35, and 36. (1944): Ibid., pt. 111, pp. 4 Hall. J., and Clarke, J. &I. ' (1894): Introduction to the Stutlp of the Genera of Rrachiopoda (Canadian species); Pal. Nicholson, H. A. New York, 8. 1 (1875): Palreontology of 01 Hinde. G. J. Okulitch. J. V. (1889): On a New Genus of Siliceods Sponges from the 'I'renton Formation at Ottawa; (1935): Fauna of the RlacL Can. Rec. Sci. 3, pp. 396-399. No. 6, pp. 96-10; (1937): Notes on Fletcherio Hudson, G. H. Trans. 21, ~t.2, ' (1907): On some Pelmatozoa from the Chazy Limestone of New York; New York State 1 (1938): Some Black River MUS. null. 107, pp. 97-131. pp. 87-111. ' (1911): Studies of Some Early Sil~rianPelmatozoa; New York State Mus. Bull. 149, - - pp. (1942): New Pterygometo~ 195-272. Canada, Proc. a (1912): A Fossil Starfish with Gmhulnrrnl Covering Plates; Ottawa Nat. 26, pp. 21-27. 45- 52. Owen, R. (1913): (1852): Descriptiorls of the Does the Type of Protopaleaster norro~cayiPresent an Oral or an Aboral Aspect; of Canada; 1,onl Ottawa Nat. 27, pp. 77-84. ' (1913): The Use of the Stereogram in Paleobiology; New York State Mu. Bull. 164, Perks, W. A. DD... 103-114. (1928): Faunas and Strat) (1915): The Genus Urasterella, with Description of a New Species; New York State Mus.. Southern Ontar 69th Ann. Rept., pp. 117-139. pp. 39-92. - - -- Notes on Urasterella pulchella Billings; Ottawa Nat. 28, p. 130. Penhallow, D. P. - Some Fundamental Types of Hydrospires, with Notes on Porocri71us sntilhi Grant; (1896): Contributior~s to New York State Mus. Bull. 177, pp. 163-166. Wharf; Roy. SO. (1925): Improved Technique in Illustration; Jour. Geol. 33, pp. 642-657. Raymond, P. E. (1927): The Surface Characteristics of Ast~oc~stites(Steynnobla.vf7~s) ottawae~rsis; Vermont, 1 (1905) : The Trilobites of Geol. Surv., Rept. 1.5, pp. 97-110. --- 1 The fauna of the t!lc Province r~fQuebec; Denlaon daekel, 0. '(1899): Stamm. Pelmatozo:~, Pt 1. 'l'hecoidea and Cystoidea, pp. 46, 50, 234, and 277. 1111I>escril)tiol~ of Thresherodiscus Jones, T. R. (1858): Notes on Palaeozoic Bivalved Entomostraca; Ann. Nat. Hist. 3, ser. 1, pp. 244-248. p11. 69-79, Si9'1, 101-111. - 'On the Palreozoic Bivalve Entomostraca of Canada; Geol. Surv., Canada. Can. I'niv. Sci. Lab., Bull. 18, pp. 340- Org. Rem. dec. 3, pp. 91-102. (1891): On some Ostracoda from the Cambro-Silurian, Silurian, and Devonian Rocks.- A. ; Geol. Surv.. Canada, Mem. 83. From the Cambro-Silurian Rocks; Geol. Sat. Hist. Surv., Canada, Contr. Can. rinurus; Denison Univ. Bull. 19, Micro-Pal., pt. 111, pp. 62-71.

.rn Missouri; Denison Univ. Sci. (1917): Recent and Fossil Itipple-mark; Geol. Surv., Canada, Bull. 25, pp 13, 34, 35, 37. and 44. and Pls. 4, 21-23, and 27. 11 Lichadilae; Amer. Jour. Sci. 4, (1926): A comparison of Recent and Lake Champlain Stages of MrKay Lake as Diatom Habitats; Can. Field Kat. 40, pp. 83-84. Faunas; Can. Nat. 36, No. 5. (1928): A Crustacean New to the Pleistocene Fauna of Canada; Can. Pield Nat. 42. No 9. pp. 211-212. Geol. Surv., Canada, Mem. 138. iso on Univ. Sci. Lab., Bull. 20, Knight. J. Brookes (11): Palaeozoic Gastropod Types; Geol. Soc. Amer., Spec. Pap. 32. .; Denison Univ. Sci. Lab.. Bull. Lambe, L. M. (1897): Description of a New Genus of Polyzoa from the Trenton Limestone at Ottawa; sota, Wisconsin, Michigan, and Can. Rec. Sci. 7, pp. 1-3. 1 (1899): A Revision of the Genera and Species of Canadian Palreozoic Corals - The Madre- pararia, Perforata and Alcyonaria; Geol. Surv., Canada, Con. Can. Pal. IV, pt. 1. l(1900): 1bid.- The Madreporaria Aporosa and the Madreporaria Rugosa; ibid., pt. 2. liver, and Trenton Formations, Logan, Sir Wm. E. iurv., Canada, Con. Micro-Pal.. (1852): On the Footprints Occurring in the Potsdam Sandstone of Canada; London Quart. Jour. Geol. 8, pp... 199-213. (1861): On the Track of an Animal L~telyFound in the Potsdam Formation; Can. Nat. 5. pp. 26-31. pp. 279-285; Amer. Jour. Sct. (2) 3, pp. 17-23. awa Field Nat. Club I. Trs. 2, (1889): Ibid., republished; New York State Mus., 42nd Rept., pp. 30-34. Miller, A. K. L-45, 69-70, 105-107, 118, 150, 1 (1943): Ozarkian and Canadian Cephalopods - Pt. 11, Brevicones; Geol. Sac. Amer., . 29, 35, and 36. Spec. Pap. 49, p. 51. '(1944): bid., pt. 111, pp.-47, 79-80, 82, 95, 109, 116. iopoda (Canadian species); Pal. \ Nicholson, H. A. ' '(1875): Palseontology of Ontario, pp. 7, 8, 10, 12-14, 16-19

------.. - . . Trenton Formation at Ottawa; ' (1935): Fauna of the Black ltiver Group in the Vicinity of Montreal; Can. Field Nat. 49. No. 6, pp. 96-107. (1937): Notes on Fletcheria incerta (Billings) and Fletcheria sinclairi n.sp.; Roy. Can. 1st.. Trans. 21, pt. 2, No. 46, pp. 313-316. .~fNew York; New York State .. (1938): Some Black River Corals; Roy. Sac., Canada, Proc. and Trans., 3rd ser. 32, see. 4, w York State Mus. Bull. 149. pp. 87-111. '(1942): New Pterygometopinae from the Ordovician of Ontario and Quebec; Roy. Sac.. es; Ottawa Nat. 26, pp. 21-27. Canada, Proc. and Trans., 3rd ser. 36, sec. 4, pp. 99-106. Owen, R. t an Oral or an Aboral Aspect; (1852): Descriptions of the Impressions and Footprints of the Protichnites from the Potsdam of Canada; London Quart. Jour. Geol. 8, pp. 214-225. w York State Mus. Bull. 164. Parks, W. A. (1928): Faunas and Stratigraphy of the Ordovician Black Shales and Related Rocks, in Species; New York State Mus.. Southern Ontario; Roy. Sac., Canada, Proc. and Trans., 3rd ser. 22, sec. 4. pp. 39-92. . 28, p. 130. I Penhallow. D. P. tes on Porocrinus smithi Grant; (1896): Contributions to the Pleistocene Flora of Canada - Nodules from Besserer's Wharf; Roy. Sac., Canada, Proc. and Trans., 2nd ser. 2, sec. 4, pp. 64-66. pp. 642-657. oblastus) ottawaensis; Vermont, Raymond, P. E. (1905): The Trilobites of the Chazy limestone; Carnegie Mus. Ann. 3, pp. 328-386. - 1 The fauna of the Chazy Limestone: Amer. Jour. Sci. 20, pp. 353-382. Ravmoncl. P. F: " ---r- - Roemer, '(1906): The Chazy Formation and Its Fauna; Carnegie Mns. Ann. 3, pp. 498598. F. 1 (1f476): Lethrea geognostica. Pt. '(1908): The Gastropoda of the Chazy Formation; Carnegie Mus. Ann. 4, pts. 3 and 4. Salter, J. W. pp. 171, 178, 186, 191, 193, 204. 1- (1853): Fossils from the Ottawa (1910): Notes on Ordovician Trilobites - 11, Asaphidie from the Beekmantown; Carnegie (1858): on Cyclocystoides, a N Mus. Ann. 7, pp. 35-45. Silurian--.- Rocks; Geol Notes on Ordovician Trilobites - IV, New aud Old Species from the Chazy; Ibid., pp. 60-80. w (1859): Canadian Organic Rem (1910): On Two New Trilobites (Bathyurus superbus and Isotelus arertieola) from the Chazy Schubert, R. J., Waagen, L. near Ottawa, Ontario; Ottawa Nat. 24, pp.- - 129-134. (1904): Die untersilurischen 1 Preliminary Notes on the 'Chazy' Formation in the Vicinity of Ottawa, Ontario; PI. 1, figs. 1,2, and ' Ibid., pp. 189-197. (1911): Chazy Formation in the Ottawa Valley (Abst.); Geol. Soc. Amer., Bull. 22, pp. Schuchert. C. 1 (1915): Revision of Palaeozoic 719-720. - . . - - . Asteroidea; U. S. N: - The Brachiopoda and Ostracoda of the Chazy; Carnegie Mus. .4nn. 7, pp. 215-259.

- (1912): Ordovician of Ottawa Valley; Geol. Surv', Canada, Sum. Rept. 1911, pp. 351-356. Schuchert, C.. and Cooper, G. A. 1 ( 1932): Brachio~odGenera c --- On Two New Pal=ozoir Starfish (one of them found near Ottawa) and a New Mus. Nat. Hist., M Crinoid; Ottawa Nat. 26, pp. 77-81. ---- On the Nature of the So Called 'covering plates' in Protoprrl~aster narrawayi; Scudder, S. H. (1896):. A Caddis-Fly from th Ottawa Nat. 26, pp. 105-108. Sci. 6, pp. 276-277. ---- Notes on Parallelism among the Asaphid=; Roy. Soc., Canada, Proc. and Trans., 3rd ser. -5, pp. 111-120. Sinclair, G. W. 1 (1940): A Discussion of the ( (1913): Ordovician of Montreal and Ottawa; Geol. Surv., Canada, Inter. Geol. Congr. XII. Soc., Canada, Pro< Gaide Bk. 3, pp. 137-162. 1 (1942): The Chazy Conularil ---- Some Changes in the Names of Genera of trilobites; Ottawa Nat. 26, pp. 137-142. -- 1 (1w): Some Ordovician Tri A Further Note on Cryptolitht1~versus Trirrucleus; Ottawa Nat. 27, pp. 26-30. pp. 15-20. ---- Notes on Cycloeystoides; Geol. Surv., Canada, Mus. Bull. 1, No. 4, pp. 23-32. 1 (1945): Notes on the Gener: Notes on Some New and Old Trilobites in Victoria Memorial Museum; Ibid., and Trans.. 3rd se No. 5, pp. 33-39. __ 1 Some Ordovician Lit Description of Some New Asaphidze; ibid., So. 6, pp. 41-48. pp. 55-82. Two New Species of Tetradium; Ibid., Xo. 7, pp. 49-50. Sowerby, G. B. A Revision of the Species whicah have been lleferretl to tlrt. (;enus Bathyurus; (1826): Notice of a Fossil B* Ibid., No. 8, pp. 51-69. Zool. Jour. 2, pp. -. Correlation of the Middle Ordovici:u~ liormations of Ontario ;rrrtl Quebec (Abst.); Geol. Soc. .imer., Bull. 24, p. 111. Sowter, T. W. E. l (1914): Table Middle Ordovician; Geol. Surv., Canada, Sum. Hept. 1912, p. 348. (1887): Report of the Geo Field Nat. Club ---- .4 Bentricecl-like Organism from the middle Ordovician; Geol. Surv., Canada, Mus. Bull. (1888): preliminary Notes 5. pp. (1915): Revision of the (:anadiar~ Species of "~igelacrinites"; Otta\v;l Nat. 29, pp. 53-62. 11-15. ' (1916): The Pelecypods of the Chazy Pormation; Carnegie Mus. .inn. 10, pp. 325-343. Springer, F. 1 Cleiocrinus; ( - .4 New Cera~~rzrsfrom the Chazy; New York State hfus. Bull. 189, pp. 121-126. (1905): - 1 (1911): On a Trenton Ech: The Genera of the Odontopleuridie; Ottawa Nat. 29, pp. 135-139. and 37. I (1917): Reecher's Classification of Trilobites after Twenty Tears: .irnrr. .Tour. Sci. (4) 43, PD. 196-218. 1 (1920): The Crinoidea Fie See also Wachsmu (1920): 'I%;.4ppendages, .Inatomy and Relatiorlships of Trilobites; Connecticut Acad. Arts, Sci., hlem. pp. 7, 34-39. Sproule,1 (19%): J. C. A Study of the C 1921): .I Contribution to the Descriptio~~of the Fauna of the Trenton (iroup; Geol. Surv., Canada, Mus. Bull. :31. 1921 Stewart, J. Raymond, P. E., and Barton, D. C. (1887): Notes on Geologia ' (1913): A Revision of the .4tuerica11 Species of ('rrctltrr~x; ~ICIS.('oirrp. Zool., Bull. 3, pp. 525-543. Teichert, C. 1 (1933): Des Bau der Act Raymond, 1'. E., and Narr;~way,.I. E. (1906): 11 New .4rnerican L'ybele; Carrlegie Mus. .-Inrl. 3, pt). 599-604. Ulrich, E. 0. 1 (1889) : On Li~igulas?lla, (1908): Notes on Ordovician Trilobites - Illenidz from the Black River Limestone near Amer. Geol. I! Ottawa, Canada: Carncgie Rlus. Ann. 4, pp. 242-255. (1910): Notes on Ordovici:~~~Trilobites - 111, Asaphitl;~. from the I.owville and Black Wachsmuth. C.. and Springer. River; C:trnrgir ~~IIR.Ann. 7, pp. 46-59. 1 (1883): Remarks on Glyl Iieed, v. It. (;o\\-pcr Amer. Jour. S (19281: Notes OII tl~eI:a~~nil~ E11cri11l1ridae: Gt.01. Miifi. 65. pp. 51-77. 1 (1897): North American Ilir~gueberg.ti. N. Weller, S. I (1889): 'l'tie ('~il(~eocrir~i(I~t~.:I 1ievisio11 of Fan~ilj-,wit11 l)tx.riptio~~of Sotne New Species; 1 (1900): Morphology of Sew \'c,rk .\c:rtl. Sri. 4, pl). :iU:i. :395. MUS. .-~IIII.3. pp. 498-698. Itoemer, P. '(1876): I~thrrageognostica, Pt. 1, Lethrea pa1;eozoica; Atlas, 1'1. 11. fig. 6. '~egiesfus. Ann. 4, pts. 3 alld 4, Salter, J. W. Fossils from the Ottawa River; Can. Jour. 1, pp. 221-222. . from the Brekrrlantown; Carnegie 1 (1853): (1858): On Cyclocystoides, a New Genus of Echinodermata from the Lower and Middle ''d Old Species from the Chazy; Silurian Rocks; Geol. Surv., Canada, Can. Org. Rem. dec. 3, p. 89. (1859): Canadian Organic Remains; Geol. Surv., Canada, dec. 1. lsotelux urett ;cola) from the <:hazy'd )-134. Schubert, R. J., Waagen, L. ' (1904): Die untersilurischen Phyllopodengattungen; Jahr. geol. Iteichsanst., pp. 42-44. the Viciuity of Ottawa, Ontario; PI. 1, figs. 1, 2, and 4.

; (;eel. Soc. .%rner., Bull. 22, pp. Schuchert. C. 1 (1915): Revision of Pal~~ozoicStelleroidea, with Special References to North America ""legie Nus. :inn. 7, pp. 215-259, Asteroidea; U. S. Nat. Mus., Bull. 88, pp. 165, 178, 219, 220. 1% Sum. Hept. 1911, pp. 351-356. Schuchert, C., and Cooper, G. A. 'olrnd near Ottawa) and a New . '(1932): Brachiopod Genera of the Suborders Orthoidea and Pentameroidea; Peabody Mus. Nat. Hist., Mem. IV, pt. 1. ?" ill /'rotol~~1/fraa6ernarrawayi; Scudder, S. H. (1896): A Caddis-Fly from the Leda Clays of the Vicinity of Ottawa, Canada; Can. Rcc. SO^., can ad:^, Pror. and Trans., Sci. 6, pp. 276-277. Sinclair, G. W. Canada. 111tc.r. Geol. Congr. XII, 1 (1940): A Discussion of the Genus Metaconularia, with Descriptiolls of New Species; Roy. Soc., Canada. Proc. and Trans., 3rd ser. 34, sec. 4, pp.- - 107-108.

cs; Ottawa Nat. 26, pp. 137-142. 1 (1942): The Chazy Conularida and their Cogeners; Ann. Carnegie Mus. 29, pp. 224-225.

' Ottawa Nat. 27, pp. 26-30. 1 (1944): Some Ordovician Trilobites from Ontario; Roy. Can. Inst., Trans. 25, pt. 1, No. 53. s. Bull. 1, No. 4, pp. 23-32. pp. 15-20. Notes on the Genera Arch~oconulariaand Eoconulnria; Roy. Soc., Canada, Proc. !aria Memori;tl Museum; Ibid., 1 (1945): and Trans., 3rd ser. 38, sec. 4, p. 92. )p. 41-48. ---- 1 Some Ordovician Lingulid Brachiopods; Roy Soc , C'tnadn, drd ser 30. sec 4, >-50. pp. 55-82. erred to tht, (;ellus Bathyurus; Sonierby, G. B. (1826): Notice of a Fossil Belonging to the Class Radiara, found by Dr. Bigsby in Canada; of Ontario and Quebec (Abst.); Zool. Jour. 2, pp. 318-320. Sowter, T. W. E. m. Rept. 1912, p. 348. (1887): Report of the Geological Branch of the Ottawa Field Naturalist Club; Ottawa

Sian; Geol. Surv., Canada, Mus.. Field Nat. Club 11, Trs. 7, pp.- > 342-349. (1888): Preliminary Notes on the Chazy Formation at .iylmer, P.Q.; Ottawa Nat. 2. s"; Ottawa Nat. 29, pp. 53-62. pp. 11-15. e Mus. Anu. 10, pp. 325-343. Springer, F. e Mus. Bull. 189, pp. 121-126. 1 (1905): Cbiocrinus; Mus. Comp. Zool., Mem. 25, pt. 2. !9, pp. 135-139. 1 (1911): On a Trenton Echinoderm Fauna; Geol. Surv., Canada, Mem. 15-P, pp. 10, 11,25. Years; -4mer. Jour. Sci. (4) 43, and 37. 1 (1920): The Crinoidea Flzxibilia; Smith. Inst., pp. 345-348, PI. 45. Trilobites; Connecticut Acad. See also Wachsmuth and Springer. .le Trenton Group; Geol. Surv., Sproule, J. C. a(1936): A Study of the Cobourg Formation; Geol. Surv., Canada, Mem. 202, pp. 93-118. Stewart, J. (1887): Notes on Geological Work During the Summer of 1887; Ottawa Nat. 1, pp. 170-171. Mus. Clamp. Zool., Bull. 54, Teichert, C. 1 (1933): Des Bau der Actinoceroiden Cephalopoden; Palaeo~ltogra~hica78, Abt. A, p. 133. 599-604. Ulrich, E. 0. Black River Limestone near 1 (1889): On Lingulasn~a,a new Genus, and eight new species of Lingula and Tremntis; .%. Amer, Geol. 111, pp. 377-390. corn the Lowville and Black Wachsmuth. C.. and Springer, F. 1 (1883): Remarks on Glyptocrinus and Reteocrinus, Two Genera of (Lower) Silurian Crinoids; Amer. Jour. Sci. (3). , 25, --PP. 262-265. I (1897): North American Crinoidea; Mus. Comp. Zool., Mem. 20. ription of Some New Sbecies; Weller, S. 1 (1900): Morphology of Crinoidea; Chicago Acad. Sci. Nat. Hist. Surv. 4, p. 28. Whiteaves. J. F. (1883): Note on the Occurrence of Siphonotreta scotica Davidson in the Utica Formation. near Ottawa; Can. Nat. Geol.. N.S. 10, pp. 396-397. (1897): Description of a New Genus and Species of Cystideans from the Trenton Limestone at Ottawa; Can. Rec. Sci. 7, pp. 287-292, 395. (1898): On Some Fossil Cephalopoda in the Museum of the Geological Survey of Canada; Ottawa Nat. 12, No. 6... D. 116. (1903): Description of a New Species of Matheria from the Trenton Limestone at Ottawa; Ottawa Nat. 17, No. 2, pp. 32-34. Notes on some Canadian specimens of Lituites undatus; Ibid., pp. 117-122, 161-163...... Acid towers, stone...... for (1904): The Canadian Species of Trocholites; Ottawa Nat. 18.- DD... 13-14. Adirondack mts...... (1906.): The Canadian Species of Plectoceras and Barrandeoceras; Geol. Surv., Carurds. Pal. Alexandria, Ont...... Foss. 111, pp. 311, 312, 316. Alfred springs...... From the Trenton Limestone of Ontario and Quebec; Ibid.. pp. 316-323. Alfred tp. Allumette is...... (1908): Notes on the Pelecypoda or Bivalve Mollusca of the Chazy Formation in Canada. Almonte, Ont...... with Descriptions of one New Genus and four New Species from the Chazy Ami, H.M...... Sandstone at Hog's Back near Ottawa; Ottawa Nat. 22, pp. 105-115. Analyses of springs ...... Appalachian movements ...... Whittaker, E. J. Arctic regions...... (1918): The Relationship of the Fossil Marl Fauna of MacKay Lake, Ottawa, to the Present Amprior, Ont...... Molluscan Fauna of the Lake; Ottawa Nat. 32, pp. 14-18. Artesian wells ...... (1922): The Fossil Mollusca Faunas of the Marl Deposits of the Ottawa District; Geol. Ashdad, Ont...... Surv., Canada, Bull. 33, pp. 59-78. Ashton, Ont...... Aylmer, Que...... Whittinadon. El. H. Aylmer formation ...... (l9Gl): ' The Trinucleidae - with special reference to North American genera and species; ...... dour. Pal. 15, No. 1, pp. 21-41. Baffin is ...... Banff Springs,...... Alta. Wilson, A. E. Barnhart is...... A New Brachiopod from the Base of the Utica; Geol. Surv., Canada. Bull. Bathyurus zone. (1913): Mus. 1, Bear Creek, Ont...... pp. 81-86. Beauharnois, Que...... (914: A Preliminary Study of the Variations of the Plications of Parastrophe'a hemiplicatu Beauharnois, anticline ...... Hall; Geol. Surv., Canada, Mus. Bull. 2, pp. 131-139. Axis...... 12 (1915): A New Ordovician Pelecypod from the Ottawa District; Ottawa Nat. 29, pp. 85-86 Canal...... Formation ...... (1921): The Range of Certain Lower Ordovician Faunas of the Ottawa Valley, with Des- ...... criptions of Some New Species; Geol. Surv., Canada, Bull. 33, pp. 19-57. Heckett is ( An Upper Ordovician Fauna from the Rocky Mountains, British Columbia; Geol. Reekmantow11 formation, correl: ' 1926): of ...... Surv., Canada, Bull, 44, p. 34, PI. 3, fig. 6, P1. 4, fig. 5. Belle Rivibre, Que...... (1932): Palsontological Notes; Can. Nat. 46, pp. 133-140. Billings, Elkanall...... - Ordovician Fossils from the Region of Cornwatl; Roy. Soc., Canada, Trans. 3rd Billings formation ...... ser., sec. 4, vol. 26, pp. 373-404, 6 pls. Wells ...... ( 1944, : Rafinesquina and its Homomorphs Dpikina and Opikinella from the Ottawa Lime- Billings Bridge, Ont.. Black River formation ...... stone of the Ottawa-St. Lawrence Lowland; Roy. Soc., Canada, 3rd ser. 38...... sec, 4, p~.. - 145-203. Blanche r.. Bonnecbbrt* r...... (1945): Strophomena and its Homomorphs Trigrammaria and Hicrotrypa from the Ottawa brings ...... Limestone of the Ottawa-St. Lawrence Lowland; Roy. Soc., Canada, 3rd ser. 39, ...... set. 4, pp. 121-150. Rorthwick springs Rrockville, Ont...... (1946) : Echinodermata of the Ottau~a Formation of the Ottawa-St. Lawrence Lowland; Brockville region ...... Geol. Surv., Canada, Bull. No. 4. Buckingham, Que...... Woodward, H. Burling, L.D...... 1 (1871: On the Structure of Trilobites; Geol. Mag. 8, pp. 289-294. Calabogie 1 ...... (1880): Notes on the Anomalocystidae; A Remarkable Family of Cystoidea Found in the Calder, J.A. Caledonia Springs, Ont...... Silurian Rocks of North America and Britain; Geol. Mag., N.S. dec. 2, vol. 7, ...... DO.193-201. Calumet is.. .. Ca~marotoechia...... (1889): On the Discovery of Turrikpas in the Utica Formation (Ordovician) of Ottawa. (:amarotoechia orientalis ...... Canada; Geol. Mag. dec. 3, vol. 6, pp. 271-275. plena ...... (:ambrian ...... Kcmdward, H., Duncan, P. M., Etheridge, R...... (1872): On the Canadian Trilobite with Leg*; Can. Nat. Geol.. N.S. ti, pp 227-231. Upper Canada Cement Company ..... Canadian Shield ...... 1. 5 Canal construction, stone for ... Cap St. Martin ...... (hrillon canal ...... C'arleton 1'Iac.t. 0111...... Davidson in the Utica porrnation. 96.397 . tideans from the Trenton Limestone

the Geological survey of Canada; INDEX

the Trenton Limestone at Ottawa; l'.iC.E 1' A<; E rndatus; Ibid.. pp . 117.122. 161.163. Acid towers. stone for ...... 36 Carlsbad. Ont ...... 15 at . 18. pp . 13.14 . Adirondack mts ...... 1, 5. 7 Carlsbad formation ...... 48 ...... 'deoceras; Geo1. Surv., Canada, pal. AlfredAlexandria, springs Ont ...... 17, 3919 Carp, Carlsbad Ont Springs, ...... Ont 20, 25, 38, 3912 Alfred tp...... 38 Cascade pt ...... :j(i !uebec; Lbid., pp . 316.323 . Allumette is ...... 16, 22 Castor r ...... 26 the Chazy Formation in Canada. .4lmonte. Ont ...... 12. 15 Chaleur Bay region ...... 31 Our New Species from the Chaay Ami, H.M...... 3 Champlain basin ...... 20 a Nat . 22, pp . 105.115 . Analyses of springs ...... 38. 39 Deposits ...... 27, 28 Sppalachian movements ...... 31 Champlain 1...... 2 Arctic regions ...... 8, 48 . 26 Area ...... 17. 20 'cKa~Lake, Ottawa, to the Present Arnprior, Ont ...... 16, 23, 29 Champlain Sea ...... 28. 3.5. 3; ., pp. 14.18 . Artesian wells ...... 38 Champlain Valley ...... 7 sits of the Ottawa District; ~~~l. Ashdad, Ont ...... 23 Chaudi&reFalls ...... 6, 22 Ashton, Ont ...... 18 Chazy formation ...... 7, 17.21. 26, 40 Aylmer, Que ...... 9. 4(j Correlation of ...... 20 Aylmer formation ...... 4.i Clarence ck ...... 48 lrth American genera and species; Baffin is ...... qg Clear. I ...... 23, 47 Banff Springs, Alta ...... 38 Cobourg member ...... 22, 23 ~~~~h~~~is ...... 1') Collingwood age ...... 23, 25 36 Bathyurus zone ...... 21 Concrete blocks ...... ;eel. Surv .. Canada. Mus . ~~11.1. Bear Creek, Ont ...... 24. 48 Ont ...... 6 Beauharnois, Que ...... 11, 16. 3(i Constance ck ...... 6 !ations of Patast~o~hiahelniplicalu Beauharnois, anticline ...... 1. 2. .5 ...... t1.139 . ~~i~ ...... 12, 13, 15, 30 Corr~wall.Ont ...... 18, 20. 27. 34. 40 istrict; Ottawa Nat . 29, pp . 85.86. canal...... 14 Credit r . valley ...... 27 Formation ...... 14 C~yptolitht~szones ...... 26 of the Ottawa Valley, with Des- 18 Cryptozoo11s ...... 14 'anada Bull . 33, pp . 19.57 . Beckett is ...... Beekmantown formation. correlation Cumberland. Ont ...... 17 'untains, British Columbia; of ...... 7. 10-17 Cumberland tp ...... 26 4 fig 5 . . . Belle RiviBre. Que ...... 11 Desch&nes,1 ...... 6 Billings, Elkanah ...... 2 Devil's Garden ...... 34 ; ROY. Sot.. Canada . Trans . 3r,j Billings formation ...... 24. 48 Diamond Park spring ...... 38 Wells ...... 24 Dolomite. Grenville and Oxford ...... 32. 34 ...... 'pikinella from the Ottawa ~i~~- Billings Bridge, Ont ...... 24, 37 Dom~n~on...... sprlng 38 OY Soc.9 Canada. 3rd Her 38, ~l~~kRiver formation 7. 20-2'3 DorC, 1 26 . ~l~~~h~r ...... 28 Douglas, Ont ...... 16, 21, 22 Bonnechere r ...... 16 Dundas-Lorraine ...... 28. 30 and Microtrypa from the Ottawa ~~~i~~~...... 17 Dunrobin. Ont ...... 14 I; Roy . Sot., Canada, 3rd ser . 39, Borthwick springs ...... 3'3 Eardley fault ...... 5, 28, 29 Brockville, Ont ...... 2. 15 East Hawkesbury tp...... 20 Ottawa.St . ~awrenceLowland; Brockville region ...... 10, 13 Eastview, Ont ...... 24.34 Buckingham, Que...... 36 Eastview formation ...... 23, 24 Burling . L.D...... 3 Eccliomphalus ...... 16, 17 89-294 . Calabogie 1 ...... 23 Eccliomphalus cal~ferus...... 16 Calder, J.A...... 4 Eganville. Ont ...... 16. 23, 36 mil^ of Cystoidea Pound in the Caledonia Springs. Ont ...... 38. 39 Ells. R . W ...... 2, 3 Geol- Mag., N.S. dec. 2, rol . 7. calumet is ...... 13 Ellwood, Ont ...... 24 Camaroioechia ...... 18 Esmonde, Ont ...... 23, 47 mation (Ordovician) of Ottawa. Camarobechia orientalis ...... 19. 20 Fairmont Springs, B. C ...... 38 plena ...... Fault blocks ...... 6 cambrian ...... 7 Faunal association ...... 24, 26 upper...... 16, 17 Ferrosilicon alloys ...... 36 "01 .. N.S. 6. pp . 227.231 . Canada Cement Company ...... 21, 34. 35 Finch, Ont ...... 22 Canadian Shield ...... 1. 5, 9. 28. 30, 32 Finch tp...... 36 Canal construction, stone for ...... 33 Fitzroy Harbour. Ont ...... 10, 12, 18, 19, 47 Cap St. Martin ...... 45 Fluvial. muds ...... 27 Carillon canal ...... 33 Foster's quarry ...... 34 Carleton Place. Ont ...... 13. 36 Fournier. Ont ...... 48 64

INDEX-CON~D

PAGE PAQE Fourth &ate of the Bonnechire ...... 23,36 Lochaber Gore tp...... 33 Papineauville. Que ...... Frontenat axis ...... 1, 2, 5, 7, 12, 28 Logan, Sir Wm...... I Parks. Mr ...... Gaspe region...... 31 Lorralneage ...... 7 Parliament Buildings of Canada .... Galetta, Ont...... 15 Lower Ordovician age ...... 7 Payne r...... Gatineau r...... 28 ~owvillemember...... 22, 23 Pembroke. Ont...... Gatineau valley ...... 28 MacLaren Landing ...... 17 Perth, Ont ...... Georgian Bay region...... 7, 48, 26 Manitoulin is...... 23 Pholadomorpha...... Giroux, N. J...... 3 Map-units...... 1 Plantagenet, Ont...... Glacial deposits ...... 8, 27 March formation ...... 12, 14 Plantagenet Springs, Ont...... Glass...... 36 March tp. 6, 10, 13, 15 Pleistocene ...... Champlain deposits ...... Gloucester, fault 9, 12, 14, 18, 25-29, 27, 30, 37 Marine beds ...... 8, 27, 28 Formation...... 23, 25 Melocheville, Que...... 36 Glacial deposits ...... Godmanchester tp...... 15 Merrickville. Ont...... 15, 34 Potsdam ...... Grabens ...... 30 Mexico, Gulf of. 8 Precambrian...... Fault Green ck. 19, 21, 22, 28, 38 Middle Ordovician ...... 7 Knobs ...... Section east of ...... 19 Mille Roches quarries...... 33, 34 11, Grenfel Tickle ...... 48 Mirabel, Que...... 32 Ridge...... Grenville, canal ...... 33 Mohawkian. 23 Rocks...... 5-12, 16, ...... Shield...... Dolomite...... 32 Montreal, Que. 22, 33, 34, 36, 38, 45, 46, 47 Fault ...... 29 Region...... 7, 45 Pr@tu8...... Limestone ...... 34 Road ...... 22 Quaternary ...... Series ...... 32 Mountain tp...... 14 Deposits ...... Sub-province ...... 32 Mud-cracks ...... 46 Quebec, Que...... 0 1...... 4 Mud 1...... 6 Queens Park...... Harding, Mr...... 11, 16 Murray, Alexander ...... 2 Queenston formation. Hawkesbury, Ont ...... 33, 38 Ncpean sandstone ...... 32 Radium emanations ...... Hawkesbury springs ...... 39 Nepean tp...... 10,12, 13, 15, 32 Raymond. P. E...... Recent deposits ...... Hawthorne, Ont...... 38, 39 n'ew York...... 16, 36 ...... Hazeldean fault ...... 12, 14, 26, 27 Niagara Peninsula...... 27 Renfrew, Ont. Relertella...... 9 Nicolet valley...... 25 Richmond, Ont...... Homotoma ...... 16 North Nation r...... 28 Richmond formation ...... Hull, Que...... 21, 22, 29, 33, 35 Sorth Plantagenet tp...... 18, 24 Rideau Lakes...... Hull member ...... 22, 23 Wells in...... 19 Rideau r...... Hurdman Bridge, Ont...... 2.5 Oyygites latima~ginatus...... 24 Rigaud, Que...... Inliers ...... 5, 47 Ontario, 1...... 28 Rigaud mt...... 13 Palmzoic ...... 2 Ophileta ...... 16, 45 Block ...... Ripple-marks ...... International Boundary ...... 1, 5, 29 Ophileta compacta...... 16 ...... Iroquois, Ont. 15, 33 Ordovician 7, 10, 27 1tr.ckcliffe Aerodrome rd...... RQ2kcliffe formation...... Johnston, W. A...... 3, 4 Lower ...... 7 Keele,Josepb ...... 4 Middle ...... 7 Rockcliffe Park ...... Kindle, E. M...... 5, 4 Upper ...... 7, 8 Rockland, Ont...... Kings mt...... 27 Ornamental stone ...... 36 Rockland member ...... Killaloe, Ont...... 23 Ottawa, Ont...... 5, 6, 17, 19, 25, 30, .34, 38 Rock products ...... Kingston, Ont...... 23 Wells ...... 15 Abrasives material ...... Knobs, buried ...... 15 Ottawa Brick and Terracotta Co...... 37 Building stone ...... Crushed stone ...... J,achute, Que...... 11, 32, 34, 36 Ottawa formation ...... 19, 21, 23 Miscellaneous uses. Lacustrine deposits ...... 27, 28 Ottawa I...... 5, 17, 28, 36, 37, 45 ...... Lambert, Valley. 38 Sand and gravel...... J ...... 4 ...... 16, Stone for cement Laurentian Highland ...... 5 Ottawa-St. Lawrence Lowland. . 7, 29, 45, 48, ...... Leitrim, Ont...... 12, 14, 25 Stone for lime...... 31, 32, 36 Itussell, Ont...... Lenses ...... 11, 17 Economic geology ...... 32. 40 17, 2' Leptmna ...... 26 Oil and gas 40 Formation ...... Lithia spring...... Leray member ...... 22, 23 Structure ...... 29: 33 l,i&vre r...... 28 Surface of ...... 5 Township ...... Sandstone, Nepear~...... Lill, R...... 4 Ottawa valley ...... 11, 13, 15, 20, 23, 29 ...... I,imestone, Grenville ...... 34 Oxford formation ...... 14, 16 Rockcliffe St. Benoit. Que...... Lithographic...... 46 Dolomite...... 33. X4 Sprxng ...... Ottawa ...... 33 Oxford tp ...... 14 St. Martin...... 33 Oxford Mills, Ont...... 34 St. Eustache. Que...... I,ingula ...... Oxford Station, Ont. Saline spring ...... 21 ...... 15 St. Helens Isle, Montreal...... Lingulella ...... 16 Yakenham, Ont...... 12, 13, 15, 18,23, 38 St. Isidore de Prescott. Que...... I,ingulella acuminata ...... 12, 16 Pakenham tp...... 38 Little Rideau ck...... 19 Pal~ozoicinliers ...... 2 little Rideau r...... I!) 1':lmelin rnernber ...... "'2. 2:: PAGE I'.ros: PAGE ii sore tp ...... 3:1 Papineauville. Que ...... 28. 29 St. Jerome, Que ...... 1 wm ...... 1 Parks. Mr ...... 48 St. Lawrence Power and Waterways ge :...... I f Parliament Buildings of Canada ...... 10. 32 Project ...... 19 ovlcian age ...... 7 7 Payner ...... 22 St. Lawrence Lowlands ...... 1 be...... , 22. 23 i: Pembroke, Ont ...... 16, 18 St. Lawrence r ...... 5, 28. ;;3 37. Landing ...... : Perth. Ont ...... 16. 36 St. Martin formation ...... 17. 19. 20 1 1s ...... 2317 , Pholadomorpha ...... 26 Sherman Fall member ...... 22. 23 ...... 1 Plantagenet, Ont ...... 48 Shirley ck ...... 6 nation ...... 12, 14 Plantagenet Springs. Ont ...... 38. 39 Silica. Que ...... 11. 36 ...... 6. 10. 13. 1.5 [ Pleistocene ...... 8. 26. 38 Drill hole at ...... 29 js e...... 8. 27. 28 Champlain deposits ...... 27 Skead rd ...... 45 le . Que ...... 36 Glacial deposits ...... 27, 28 South Gloucester. Ont ...... 30 !e. ont...... 15. 34 Potsdam ...... 16 Springs. Alfred ...... 39 llf of ...... Precambrian ...... 9, 10 Analyses of ...... 38. 39 lovician ...... 8 Fault ...... 30 7 Banff. Alta ...... 38 es quarries ...... 33. 34 Knobs ...... 11, 12. 14. 30 Borthwick ...... 39 ue ...... 32 Ridge ...... 15. 18 Caledonia ...... 38. 39 1...... 23 Rocks ...... 5-12, 16, 28. 29, 32 Carlsbad ...... 39 Que. 22. 33. 34. 36. 38. 45. 46. 47 Shield ...... 37, 41 Diamond Park ...... 38 ...... 7. 45 l'retue ...... 26 Dominion ...... 38 ...... 22 Quaternary ...... 27, 28 Fairmont. B . C...... 38 p ...... Deposits ...... 5. 27 Hawkesbury ...... 39 4 ...... 4614 Quebec, Que...... 2 Plantagenet ...... 38. 39 ...... 6 Queens Park...... 21 Russell Lithia ...... 38 exander ...... 2 Queenston formation...... 26. 27 St. Benoit ...... 38 dstone ...... 32 Radium emanations ...... 38 St. Eustache...... 38 ...... 10. 12. 13. 15. 32 Raymond, P . E ...... 3 Winchester ...... 38. 39 ...... 16. 36 Recent deposits ...... 28 Sproule. J . C ...... 23 ~insula...... 27 Renfrew, Ont ...... 23 Still ck ...... 6 Y ...... 2.5 Richmond, Ont ...... 18 Stone for acid towers ...... 36 Bn r ...... 28 Richmond formation ...... 7, 8, 26. 27 Table of formations ...... 8 agenet tp...... 18. 24 Rideau Lakes ...... 2 ...... Theresa formation ...... 45 19 Rideau r ...... 2-2 Torbolton tp 6. 10. 15 narginatus ...... 24 Rigaud. Que ...... 1, 34 ...... Rigaud mt 13, 15, 17, 34 Toronto. Ont ...... 36 ...... Transitional beds ...... 14 Block ...... 12 Ripple-marks ...... 11, 17, 18 Trenton age ...... 7. 20. 23 Rockcliffe Aerodrome rd ...... 45 Triarthus ...... 48 Rockcliffe formation...... 17-18, 33 Two Mountaills. co ...... 40 Rockcliffe Park ...... 17, 33 Lake of ...... 1. 2 ...... 7. i( Rockland, Ont ...... 45 Upper Cambrian ...... 16. 45 toe...... 36 Rockland member ...... 22, 23 Upper Ordovician ...... 7. 8 ...... Utica age ...... 7 ...... 5. 6. 17. 19. 25. 30. 34 .... 38 Rock ~roducts 32-37 ...... 1.5 Abrasives material ...... 36 Valleyfield. Que ...... 33 k and Terracotta Co ...... 37 Building stone ...... 32, 34 Vancouver. B . C ...... 36 ation ...... 19. 21, 23 Crushed stone ...... 34, 35 Vankleek Hill. Ont ...... 19 ...... 5. 17. 28. 36. 37. 45 Miscellaneous uses ...... 36, 37 Vars. Ont ...... 26 ...... 16. 38 Sand and gravel ...... 39 Varved clays ...... 8 aawrence Lowland . . 7. 29. 45. 48. Stone for cement ...... 35 Vennor. H . G ...... 2 Stone for lime ...... 36 31. 32. 36 17,26, 30, 37, 45 Water ...... 37. 40 geology ...... 32 . 40 Russell, Ont ...... Drilling for ...... 39 Formation ...... 26. 27 Water ck ...... 6 Lithia spring...... 38 Watts ck 6 Township ...... 26, 34 ...... Sandstone, Nepeau ...... 32 Wells ...... 22. 24. 25. 47 Rockcliffe ...... 33 Whitby. Ont ...... 48 St . Benoit, Que ...... 40 Whitella fauna ...... 25. 29 Spring ...... 38 Whittaker. E . J ...... 4 St. Eustache. Que ...... 40 Wilson. M . E ...... 3 Saline spring ...... 38 Wilson .W . J ...... 4 St. Helens Isle, Montreal ...... 31 Winnipeg. Man...... 36 ...... 38 St. Isidore de Prescott . Que...... 48 Winchester Springs. Ont ...... 38. 39 ers ...... 2 ber ...... 22. 23